Fluvial Fades Analysis of Yamuna River South Mathura District (U.P.,

DISSERTATION SUBMITTED IN PARTIAL FULFILMENT OF THE REQUIREMENTS

FOR THE AWARD OF THE O^RGEE OF

Mnittx of $(}tIof(o|)tip IN

^ifl^i^#«f

BY

SHYO PRASAD

DEPARTMENT OF GEOLOGY AUGARH M U 9 L I M UNIVERSITY

ALIGARH (INDIA) 1 9 9 0

DS2063

Dr. S, M. Casshyap Ph.D. (AMU), Ph.D. (UWO, Canada) Humboldt Fellow (W. Germany) PROFESSOR OF GEOLOGY

UEPARIMENT OF GEOLOGY ALIGARH MUSLIM UNIVERSITY

ALlGARlI-202002

Phone : off. 5615 Res. 7080 TELEX: 564-230-AMU-IN

Dale 2-1.03.1991

This i s to c e r t i f y t h a t t h e research xv-orlc presented in t h i s d i s s e r t a t i o n has been c a r r i e d out by Mr. Shyo Prasad under my supervis ion at t h e Department of Geology, Aligarh Muslim Un ive r s i t y , Al igarh . The v;ork i s an o r i g i n a l con t r ibu t ion of t h e candidate cind has not been submitted for any degree at t h i s or any o the r U n i v e r s i t y .

I t i s recommended tha t Mr. Prasad may be allowed to submit the d i s s e t t a t i o n for t he award of t he degree of rlAbTER OF HlILObOHlY in GEOLOGY at t h e Aligarh Muslim U n i v e r s i t y , Al igarh .

Supervisor

C O N T E N T S

L i s t o f F i g u r e s

L i s t of T a b l e s

CHAPTER-I : INTRODUCTION

G e n e r a l Remarks

Cho ice of t h e Yamuna R i v e r

S t u d y Area

O b j e c t i v e

CHAPTER-II

CH^PTER-II I

Page No.

I

V 1

: METHOD OF INVESTIGATION

Geomorphlc F e a t u r e s

L a t e r a l a c c r e t l o n a r y b a r s

V e r t i c a l a c c r e t l o n a r y d e p o s i t

F i e l d S t u d y

L a b o r a t o r y P r o c e d u r e

: FACIES ANALYSIS

S e d i m e n t a r y F a d e s of R i v e r Yarauna

C o a r s e t o Medium Sand F a d e s

P l a n a r c r o s s - b a d d e d fac iesC Sp)

T r o u g h c r o s s - b a d d e d f a d e s ( S t )

M a s s i v e t o h o r i z o n t a l b a d d e d f a d e s

(Sm-Sh)

C h a n n e l f i l l f a d e s (Sch)

F i n e s a n d . S i l t & C l a y F a d e s

R i p p l e l a m i n a t e d t o r i p p l e d r i f t

l a m i n a t e d f a d e s (Sr)

Muddy f a d e s (Mm)

5"

5"

7

8 \o

\1

\^

\S"

\G

2 o

G e n e r a l comments •53

G r a i n S i z e V a r i a t i o n

G r a i n S i z e D i s t r i b u t i o n i n R e l a t i o n ^ t o S e d i r r e n t a r y S t r u c t u r e s

P l a n a r C r o s s - b e d d i n g s a n d f a c i e s -

L a r g e s c a l e t r o u g h c r o s s - b e d d i n g ^ ^ s a n d f a c i e s

Smal l s c a l e t r o u g h c r o s s b e d d i n g ^

H o r i z o n t a l l a m i n a t e d s a n d f a c i e s -

R i p p l e c r o s s d r i f t lamJLnated f a c i e s 5 3

V e r t i c a l V a r i a t i o n i n G r a i n S i z e S^

CHAPTER-V : HFAVY MINFRALS OP "iAMUNA RIVER SAND DESCRIPTION.

59

tt

GG

Source Rock Composition.

CHAPTHH-VI : WATER Ai D SEDIMENT POLLUTANTS

G e n e r a l S t a t e m e n t

w a t e r P o l l u t a n t s ^ ^

' Method "o f -Co l I f ec t lon t C

A n a l y t i c a l p r o c e d u r e ^ ^

R e s u l t and d i s c u s s i o n

Major e l e m e n t s a n d r a d i c a l s

T r a c e e l e m e n t s

Sed imen t P o l l u t a n t s

Method of C o l l e c t i o n

A n a l y t i c a l p r o c e d u r e

R e s u l t a n d d i s c u s s i o n

M<iJor e l emen t s '

T r a c e e l e m e n t s

SUMMARY AND CONCLUSION

L I S T OF FIGURES :

i B g e N o .

Fig. 1 : Regional map of India shoving the boundry ^

of Uttar Pradesh and study area including

importan places from Shergarh to Etawah

along river, Yamxina, western U.P.

Fig. 2 : Map showing the location of sectors (1-4)

and rivers of the study area.

m e»

Fig. 3 : Map showing the general course of the ^ '

Yamuna river at Shergarh, (Sector 1) of

Mathura district. Black dots in vertical

sections indicate location of trenches.

Fig. 4A : Photograph showing cosets and sets of cross- '

bedded sandy facies (sp) in vertical section,

showing a progressive decrease in scale of

forset from base to top.

Fig. 4B : Photograph of planar cross bedded sandy "

facies (sp) in the lower part of point-

bar cycle.

Fig. 5A : Photograph showing large scale trough cross- Av *' '2>

be elded .sand facies (St) in the lower part

and progressively decrease in scale from

P i g . 5B : Photograph showing la rge scale trough

cross bedded satid facies (St) .

t^\o n

Fig. 6 : Photograph showing snail scale trough T ' °

_ cross bedded sand /silt facies (Sr) in

the upper part of the point bar sequence.

Fig. 7 : Photograph showing horizontal laminated

sand facies (Sh) overlying this Sh-

facies is Sa-facies.

Fig. 8 : Photograph showing inclined horizontally

laminated sandy facies (Sh) .

Fig, 9 : Map showing the general course of the ^^

Yamuna river at Agra (Sector-3) . Black

dots in vertical sections indicate the

location of trenches.

Fig. 10 : Photograph showing channel-fill_, cross-bedded AflCi 2:

point bar deposit of the Yamuna river,

at Agra. On the top of the channel^ the

last phase is seen filled with layers

conforming to the shape of the channel.

Fig. 11 : Photograph showing ripple drift cross-

laminated facies (Sr) in fine to very

fine sand and silt.

Pig. 12 ; Photograph showing structureless massive M'^' ^^

Ynud ( M m ) In the middle part of the

photograph.

Fig. 13 : Photograph showing thickening of muddy

fades (Mm) towards levee deposit and

gradually thinning towards channel.

27

a7 F i g . 14 : Photograph showing la rge scale trough

cross-bedding (In the lower part) and

convolute and cross d r i f t laminations

In s i l t (upper par t ) .

F i g . 15 : Map showing the general flow of the M^^^ - ^

Yamuna r i v e r a t Mahavan (Sector 2) Black

dots In v e r t i c a l sec t ions Indica te

locat ion of t renche and exposed sect ions

(A,B,C) .

F i g . 16 : Photograph showing p a r a l l e l lamination

(Si) In the i^per pa r t . In v e r t i c a l

sequence.

F i g . 17 : Diagrams showing Log p robab i l i ty p lo t s of ^ o - ^2

grain s ize d i s t r i b u t i o n of Trench No. 1 :

a , . Trench No. 2 : b. Trench No. 3 : c,

a t Shergarh.

^5

Pig. 18 : Size frequency cumulative percent plots ^^

of Trench No. 1-3 at Shergarh. Vertical

sections on the left side showing

generalised facies model.

Pig. 19 : Diagram showing Log-probability plots of

grain size distribution of Trench-4 at

Mahavan.

Fig. 20 : Diagrams (a, b, c,) showing Log-probability A4-^^

plots of grain size distribution of Trench

5-7 at Agra.

Fig. 21 : Size frequency cumulative percent plots of

Trench No. 5-7 at '^gra. Vertical sections

(left side) show generalise facies model.

Fig. 22 : Size frequency cumulative percent plots of ^5"

Trench No. 4 at Mahavan. Vertical section left

shows generalised facies model.

LIST OF TABLES

P ^ e -no

T a b l e - 1 : Cunumlatlve frequency d i s t r i b u t i o n -*

(Percen t of Yamuna Sands .

T a b l e - 2 : S t a t i s t i c a l parameters of Sands . ^^

eg T a b l e - 3 : Percen tage of Heavy mineral Spec ies

a t d i f f e r e n t l o c a l i t y .

Ta b l e -4 : Concen t ra t ion of r a d i c a l s and major

e lements i n wa t e r s of Yamuna r i v e r

(ppm).

T a b l e - 5 : Concen t ra t ion of t r a c e e lements i n

water of Yamuna r i v e r (ppm),

t 8

G3

T a b l e - 6 : Drinking water s t a n d a r d s . ^ ^

T a b l e - 7 : Concen t ra t ion of major e lements i n g o

the sediments of Yamuna r i v e r (ppm) .

T a b l e - 8 : Concen t ra t ion of t r a c e e lements in 81

sediments of Yamuna r i v e r (ppm).

Tab l e -9 : Corrparision of c e r t a i n t r a c e elements 82

with Mean World ' s Sea sediment va lues

(ppm) .

A C K N O W L E D G E M E N T

I am highly indebted t o my Supervisor Prof. S.M.Casshyap,

Department of Geology, AUgarh Muslim Universi ty, Aligarh who

spared h i s precious time t o <xaiA.e and in sp i r e me a t each and

every s tep throughout the course of t h i s inves t iga t ion .

I am very grateful to Prof. S.H. I s r a i l i , Chairman,

Department of Geology, Aiigaorh Muslim Universi ty, Aligarh

for providing Library and .Laboratory f a c i l i t i e s for the

p re sen t work.

I am highly thankful t o Dr. K. Aslam, Pool Officer and

Dr. Adal Singh for t h e i r valuable suggestions, unfa i l ing source

of encouragement and in sp i r a t i on throughout the completion of

t h i s d i s s e r t a t i o n .

A special word of thanks i s due t o Mohd. Asif, Abdullah

Khan, B.K. Shrivastava and Akram A n Khan for t h e i r help in

ma te r i a l i z ing t h i s work.

Thanks a r e due t o Mr. H. Ahead, S,T.A. (photography),

Mr. Firoz Jawed, S,T*A, (Geochemical Laboratory) and Abdul A,Khan

(Section Cu t t e r ) . I must escpress my sincere thanks t o SO ST(U.P.)

fo r providing roe f inanc ia l ass i s tance .

Final ly , language foiils here to acknowledge my beloved

p a r e n t s , family members, who alvjays took keen i n t e r e s t ,

i n s p i r e d and helped rae in my a i l endeavour.

CHAPTER - I

INTRODaCTION

GENERAL REMARKS

The s tudy of modern f l u v i a l sediraent has a t t r a c t e d a

g r e a t dea l of a t t e n t i o n of s ed imen to log i s tS / h y d r o l o g i s t s ,

civJLl eng inee r s and geographers i n r e c e n t y e a r s . The s e d i -

mentologLsts and h y d r o l o g i s t s determine t h e t e x t u r e , bed

forms, pr imary d e p o s i t i o n a l s t r u c t u r e s , composi t ion of

a l l u v i a l depos i t s t r a n s p o r t e d by t h e s t reams, a l s o h y d r a u l i c

c o n d i t i o n s and mechanics of modern system of meandering and

b r a i d e d r i v e r c h a n n e l . As a l s o , an i n t e g r a t e d s tudy of

modern r i v e r s , t h e i r hydrology, sediment t ypes and

c h a r a c t e r s should p rov ide a b a s i s of vrorking out a f l u v i a l

f a c i e s and d e p o s i t i o n a l model, as an analogue t o g e o l o g i c a l l y

a n c i e n t f l u v i a l d e p o s i t s .

Water flovdng over l o o s e sand bed tend t o produce

bedforms in d i f f e r e n t s t a g e s i n response t o s l o p e , d i s c h a r g e

and h y d r a u l i c c o n d i t i o n and sediment supp ly . Migra t ion of

bedforms c o n t r o l s t h e movement of bed load . Thus, t h e s tudy

of bedorms, t h e i r f a c i e s , t e x t u r e , bedding type , geometry

and conposition i s an inpor tan t approach for understanding

r i v e r behaviour and raode of t ranspor ta t ion and depos i t ion .

Meandering streams of high s inuosi ty channel p a t t e r n

coiranonly t ranspor t sand with admixture of s i l t and c lay

along channel and i n adjacent subenvironraents across the

flood p la in .

The r e su l t an t sediment facies types are d i s t i n c t i v e

features of each sub-environment; t h e i r l a t e r a l migration,

through time, y ie lds a v e r t i c a l sequence of fac ies i n a

preferred and p red ic t ab le order in accordance with the

Walther 's Law of f a c i e s .

The sedimentation processes are g rea t ly influenced and

control led by t ec ton ic s e t t i n g and cl imate, p a r t i c u l a r l y

in a l luvia l b a s i n s .

The Ganga bas in of Ut tar Pradesh and Bihar, drained

by a netvrork of l a rge and small r i v e r system l i k e Yaraina,

Ganga aid Ghagra. e t c . (Fig. 1) , provides a c l a s s i c a l

example of a r c h i t e c t u r a l elements of a foreland bas in to

the south of r i s i n g Himalayas (Dickinson, 1974 b) . The

t rop ica l climate of t h i s t e r r a in accoxints for a high and

low seasonal water and sediment d ischarge . The consequent

Regional map of India showing the boundry

of Uttar rradeah and study area including

sedlmentry f a d e s of t h e s e r i v e r s a r e s i g n i f i c a n t l y \anique

and have a t t r a c t e d a g r e a t dea l of a t t e n t i o n of sedi raento-

l o g i s t s of I n d i a and abroad .

CHOICE OF RIVER YAMUNA

The choice of r i v e r Yaratma f o r t h i s r e s e a r c h work was

i n f l u e n c e d l a r g e l y b y i t s un ique geographic , g e o l o g i c , and

hydro log ic s e t t i n g , a s an analogue of a t r o p i c a l and

t e c t o n i c a l l y s u b s t a b l e t e r r a i n . I t s p rox imi ty from A l i g a r h

was t h e o the r f a c t o r i n the s e l e c t i o n of r i v e r Yamuna f o r

t h e p r e s e n t s tudy .

The ri%rer Yamuna, i n t h e s t a t e of U t t a r Pradesh, r i s e s

Vc i Himalayan range n e a r J a r a n o t r i . iSie r i v e r flows i n

s o u t h e r l y d i r e c t i o n through t h e l e s s e r Himalaya, t h e

f o o t h i l l s , and i n t h e p l a i n s of western U .P . ( F i g . 1 ) , as

i t pa s se s through t h e towns of Arobala, Yamuna Nagar, K a r a n a l ,

Son ipa t , Delh i , Mathura t o Agra. At A g r a , i t t u r n s ea s tward

and d r a i n s by Ferozabad, Stawah and Al lahabad . In the

l a t t e r s e c t o r i t r e c e i v e s a nuraber of sou thern t r i b u t a r i e s ,

l i k e t h e Charabal, Son-Betwa and Ken. Af te r a coxoxse of

about 1326 tan, Yamuna j o i n s the r i v e r Ganga a t A l l ahabad .

In a way Yamuna i s c o n s i d e r e d as t h e l a r g e s t t r i b u t a r y of

Ganga.

During the summer . season* the r i v e r Yamuna dwindles

t o a small stream i n many p a r t s owing t o sharp f a l l i n wa te r

d i s c h a r g e and p a r t l y due to e x c e s s i v e evapo ra t i on , a s a l s o

because water i s drawn of f i n t o a v a s t network of i r r i g a t i o n

c a n a l s .

STUDY AREA

The s tudy a c s a i i e s between 79" t o 78* 30 ' E. Long i tudes

and 27* 48* to 36 ' 4 8 ' N . L a t i t u d e s of wes tern U .P . The

a r e a i s d iv ided i n t o 4 s e c t o r s along t h e r i v e r cou r se f o r

t h e purpose of t h i s i n v e s t i g a t i o n , namely s h e r g a r h , Kahavan

(Gokul), Agra, and E t a w a h - ( p i g , 2 ) .

OBJECTIVS

The p r e s e n t r e s e a r c h aims a t s tudying t h e sediment

l o a d , sedimentary s t r u c t u r e s , sedimentary f a c i e s and heavy

minera l corrposi t ion, as a l s o v a r i a t i o n i n water and^sed inen t

p o l l u t i o n of r i v e r Yanuna i n t h e a r ea between Shergarh

(Mathura) 'and Agra.

F i g . 2 : Map showing the l o c a t i o n of s ec to r s (1 -4 )

and r lve rn of thi? atndy ar<?f» .

CHAPTER - I I

MEOHODS OP INVESTIGATION

GEOMDRPHIC FEATURES

In the a rea between Shergarh and Etawah, a long t h e

coxirse of r i v e r Yamuna, t he fol lowing georaorphic featxires

a re commonly obseirved.

1) L a t e r a l a c c r e t i o n a r y and marginal b a r s on concave s i d e of meander beads, and marginal b a r s a long t h e r i v e r banks .

2) V e r t i c a l a c c r e t i o n a r y d e p o s i t s on concave s i d e .

3) Veneer of wind bloMi showing t r a i n s of symmetr ical r i p p l s , and b u s h e s .

Lateral Accretionary Bars

The sedimentary f e a t u r e s on a c t i v e channel bot tom a r e

n o t e a s i l y d i s t i n g u i s h a b l e a t most p l a c e s a long

t h e cour se of r i v e r Yamuna due to water dep th and f low.

However, p o i n t b a r s and marginal b a r s a re formed as a r i v e r

channel mig ra te s l a t e r a l l y . The s e r i e s of a c c r e t i o n a r y

b a r s so developed along r i v e r Yarauna fo l low a g e n e r a l t r e n d

of the meander channel ; width i s about 50-70 m fo r t h e

outer nost bar but decreases gradually for inward bars a t

Shergarh^ Mahavan, and Agra. These f luvia l deposi ts cons i s t

mostly of sand and occupy the marginal boundaries of an

ac t ive channel close to the r i v e r bank,

iSie d i s t a l p a r t of the accretionary ba r s become

progress ively more vegetated than proximal p a r t near tha i wag.

The d i s t a l bars are approximately 300-500 m away from the

act ive channel at Shergarh suggesting a l a t e r a l s h i f t of

the e a r l i e r channel by about 300-500 m a t Shergarh, during

a span of about 15 years or so . The upper most p a r t of

l a t e r a l accret ionary bars i s a f l a t flood p la in surface

consis t ing of fine sand and s i l t ; the proport ion of s i l t

increasing in the d i s t a l accret ionary b a r s .

Ver t ica l Accretionary Deposit

Vert ical accre t ionary deposi t s develope as a r e s u l t of

s e t t i n g of suspended load from flood waters along the concave

bank of meander bend was examined carefu l ly . The cut bank

i s s tabl ized by thick c lay and veg i t a t ion . As we go upward

i t passes in to t e r r a c e s . The banks are genera l ly higher up

to 6 m than r i v e r bed.

The overbank v e r t i c a l accret ionary deposi t s cons i s t of

f i n e g ra ined sediments and a re well developed i n proximal l e v e e s

a long s t e e p e r concave bank and d i s t a l backswaraps.

Splays / a l s o c a l l e d , c revase s p l a y s , a r e a l s o i n c l u d e d

i n overbank f lood p l a i n d e p o s i t s . These d e p o s i t s a r e formed

as bed load m a t e r i a l i s accuitulated with a d j a c e n t l e v e e s ,

b rough t down l o c a l l y by channel wa te r s through c r e v a s s e s i n

overbank l e v e e s du r ing high d i s c h a r g e .

FIELD STUDY

During the field work, the object was to identify

sedimentary facies and their vertical as well as lateral

association along the course of river Yamuna in the study

area. The sedimentary facies were differentiated and examined

in p>oint bar, channel bar, and overbank areas.

The channel bars are generally accessible in shallower

convex side of meandering river or are exposed owing to fall

in water level or shifting of river course. The sandy

channel bars so exposed abound in super^imposed dunes, bars,

and ripples of varying dimension and shape. Ripple marks of

asymmetrical lunate and linguoid types commonly characterise

the active channel beds, levees,/crevasse splays.

The convex bank on shallower s ide of channel, s loping

about 2-6 degree, i s a typica l s i t e for accunulation of

accret ionary point bar , spec ia l ly i n meadering channel . A

poin t bar facies ranging from coarse to fine sand from base

to top i s often capped by t h in ly bedded f ine sand, s i l t , and

c lay to generate a finning upward sequence of va r i ab l e

thickness from l e s s than a meter to a couple of meters . The

f ining upward sequence i s considered to be a product of

l a t e r a l accretion as also ve r t i c a l aggradation due to

progressive l a t e r a l migration and f i l l i n g of the channel,

respec t ive ly (Allen, 1963) .

The r iver bank, opposite to convex bank, developed along

the deeper s i t e , forms a steeper cut bank (concave) of

meandering r iver channel, es tab l i shed by thick c lay and

overgrown veg i ta t ion . The concave bank of levees comprising

interbedded fine sand, s i l t and clay i s general ly high and

steep to v e r t i c a l , facing the ac t ive channel; i t g en t l e s down

gradual ly to become near ly hor izonta l , away from the bank

towards low lying cu l t i va t ed f i e ld and backswaitp.

The facies study was ca r r i ed out a t surface in well

exposed sections and in subsurface by digging t r enches .

Seven sanples s i t e s were se lec ted a r b i t r a r y over an area of

26 km from n o r t h to south and eas tward a t Shergarh ,

Mahavan (Gokul), Agra/ and near Etawah (F ig . 2) .

The t r e n c h e s were dug a t v a r i o u s d e p o s i t i o n a l s i t e s i n

p o i n t b a r s / c u t bankS/ and i n low l y i n g backswantps. V e r t i c a l

f a c i e s of sedminetary sequence were examined i n t r e n c h e s

bo th i n l o n g i t u d i n a l s e c t i o n s p a r a l l e l t o f low and t r a n s v e r s e l y

and s k e t c h e s were drawn to s c a l e to i l l u s t r a t e d i f f e r e n t

f a c i e s t h e i r r e l a t i o n s h i p , bedding type , t e x t u r e and p r i m a r y

sed imentary s t r c u t u r e s and geometry. Sediment s a u r i e s of

v a r i o u s f a c i e s were c o l l e c t e d v e r t i c a l l y a t s u i t a b l e i n t e r v a l s

from each t r ench for l a b o r a t o r y i n v e s t i g a t i o n of g r a i n s i z e

and heavy mineral c o n t e n t .

Surface water samples and s o i l s a n p l e s were a l s o c o l l e c t e d

from each s e c t o r for t he study of water and sediment

p o l l u t a n t s ,

LABORATORY PROCEDURE

The g r a i n s i z e a n a l y s i s was c a r r i e d ou t by s i e v i n g

samples a t 4 / 2 s c a l e of Wentworth u s i n g ASTM s i e v e s of

22 cm d iamete r , 36 samples from d i f f e r e n t l o c a l i t i e s a t

Shergarh , Mahavan (Gokul), and Agra, i n c l u d i n g 7 t r e n c h e s ,

^«rere s e l e c t e d f o r g r a i n s i z e a n a l y s i s . In each c a s e , 100 g

of sample was sieved for 15 minutes using R o - t ^ sieve Shaker

and fract ions from d i f fe ren t sieves were co l l ec t ed . The

weight percent frequency* and cuiraolative weight percentages

were cottputed and curaulative weight frequency curve p l o t t e d

for each san5>le. To determine the sediment p rope r t i e s ,

s t a t i s t i c a l parameters of s ize frequoicy d i s t r i b u t i o n given

by Folk and Ward (1957) and Visher (1967) were confuted.

13 sanples were se lec ted for heavy mineral ana lys i s . The

heavy mineral separat ion was ca r r i ed out from the f rac t ion

next f iner to modal c l a s s , using the centr i fuge method of

Taylor (1938) . The bromoforra of specif ic g rav i ty 2.89 as

separating medium was used.

CHAPTER - I I I

FACIES ANALYSIS

Modern f luvial sediments have been extensively studied

in the l a s t few decades espec ia l ly to e r e c t facies models

t ha t may be used in c lass i fy ing and descr ib ing the ancient

sediments. For example for f luv ia l sediments, facies

model may be three dimensional one as suggested by Allen (1965)

for meandering streams or may be in the form of v e r t i c a l

p r o f i l e s as proposed by Miall (1978) and Rust (1978) or

may include d i s t r ibu t ion of l i t h o f a c i e s for the e n t i r e

deposi t ional environment (Miall, 1985) . However, fac ies

models involving ve r t i c a l d i s t r i b u t i o n of l i t h o f a c i e s sho\ild

be analysed careful ly with the r e a l i z a t i o n tha t s imilar

v e r t i c a l p ro f i l e s may be produced by v a s t l y d i f fer ing

autocycl ic and a l locycl ic process .

In recent years , a l o t of information of f luv ia l

systems has accumulated and i t suggests a l l gradation in channel

morphology and re la ted l i t h o f a c i e s between end members l i k e

meandering, braided e t c . These gradation occur due to

changes in va l ley slopes, sediment load, bank mater ia l .

Also^ many f luvial processes are coraraon to various end meixber

f l u v i a l systems and gradation between them (Miall, 1985;

Bridge/ 1985) . Coraraon conponents of these various f luv ia l

depos i t s need to be defined and t h e i r i n t e rna l va r i a t ion and

re l a t ionsh ip between them need to be worked out for recons t ­

ruc t ion of various controls on f l uv i a l sedimentation. The

inves t iga t ion of tiiese common conponents in macroforras

(Jackson, 1975) in f luv ia l depos i t s i s ca l led a rchi tec t i i ra l

element analysis (AEA) by Miall (1985).

Friend (1983) proposed a scheme of c l a s s i f i c a t i o n of

f luv ia l channel a rch i tec ture based on type of bed i . e .

t r a c t i on , s a l t a t i on , suspended load streams, and mobil i ty

of channels .

In inves t iga t ion of f luv ia l sediments, a hierarchy of

var ious element and t h e i r analyses can be recognised e . g .

fac ies l i k e coarse to medium sand fac ies and fine sand,

s i l t and clay facies e t c . are the bas ic bu i ld ing of the

b l o c k s . These may be organised in to l a r g e r macroforms or

a r ch i t ec tu ra l elemeits (Miall, 1985) l i k e l a t e r a l accre t ion

depos i t s , point bar complex e t c . Next higher order u n i t s

are the main channels, which are f i l l e d by d i f f e ren t types

of elements and cal led a rch i t ec tu ra l s t y l e s by Miall (1985) .

s t i l l h ighe r order a n a l y s i s i nvo lves s tudy of r e l a t i o n s h i p

between channels and overbank d e p o s i t s and t h i s i s mainly

c o n t r o l l e d by f l u v i a l channel a r c h i t e c t u r e of F r i end (1983) .

This type of a n a l y s i s may be extended to t h e v^o le d e p o s i t i o n a l

environment . All t h e s e i n v e s t i g a t i o n have been i n c l u d e d xinder

t h e heading of " f a c i e s a n a l y s i s ^

SSDIMSM'EARY FACIES OF RIVER YAMUNA

In view of the above a s p e c t s , t h e d e t r i t a l sediments

of r i v e r Yamuna were examined i n each s e c t o r and the fol lowing

d a t a were c o l l e c t e d i n o rde r t o d e l i n e a t e t h e v a r i o u s

sedimentary f a c i e s .

1) I d e n t i f y i n g sedimentary f a c i e s on t h e b a s i s of co lour , g r a i n s i z e , bedding t y p e s , sediraenteiry s t r u c t u r e s and mode of occurence and t h e hydrodynamic regime r e s p o n s i b l e for the formation of v a r i o u s bed forms.

2) Recording and examining geometry of bedding t ypes and f a c i e s i n v e r t i c a l A i o r i z o n t a l p l a n e s i n s e c t i o n s and i n t r e n c h e s , and t h e i r digrammatic r e p r o d u c t i o n t o s c a l e , wherever n e c e s s a r y .

3) Examining sedimentary s t r u c t o r e s , and v e r t i c a l and l a t e r a l a s s o c i a t i o n of f a c i e s as p e r san5>le p l a n e .

On t h e b a s i s of f i e l d s t u d i e s , f a c i e s as a r c h i t e c t u r a l

e lements of r i v e r Yamuna were r ecogn i sed and coded i n d i v i d u a l l y

fo l lowing the modified scheme of Mi a l l (1978) . The f a c i e s are

as fo l lows :

A- Coarse t o medlxim sand f a d e s ;

1 . P l ana r c rass -bedded f a c i e s (sp)

2 . Trough c ross -bedded f a c i e s ( s t )

3 . Massive t o h o r i z o n t a l l amina t ed f a c i e s (sh)

4 . C h a n n e l - f i l l f a c i e s (sch)

B- Fine sand^ s l i t and c l a y f a c i e s :

5 , Ripple l amina ted t o r i p p l e d r i f t l amina ted f a c i e s (sr)

6 . Massive raud f a c i e s (Mm)

7 , Convolute l amina ted f a c i e s (Fc)

8 . P a r a l l e l l amina ted f a c i e s (Sl)

COARSE TO MEDIUM SAND FACIES

P l a n a r C^ross-bedded F a c i e s (Sp)

P lanar corss -bedded sand f a c i e s (Sp) i s vd.dely

developed i n the s tudy a r ea p a r t i c u l a r l y i n p o i n t b a r s as

r ecorded i n s e c t o r 1 s t a t Shergarh (FLg. 3 ) .

This f a c i e s i s grey t o vrtiite i n co lour , and occurs as

channel l i k e bod ies i n c o s e t s more than s i n g l e s e t s

( F i g , 4 A,B) . Indivtdxial t h i c k n e s s of p l a n a r c ross -bedded

se t s va r i e s on an average from 20-50 cm and shows uneven and

cxirved base and f l a t top . The laminae are commonly planar

and do not have tangent ia l r e l a t i onsh ip to the basal sxirface

of the s e t s . The inc l ina t ion of planar fo r se t s i s 18* - 25**

on an average. The channel l i k e corss-bedded (Sp) sandy

bodies are dominantly mediuun to vary fine grained (ranging in

s ize from 25 nan to .0625 mm* the graphic mean s ize (Mz), however,

var ies from .209 to .198 ran, though l o c a l l y contain subangular

to angular granviles and fine pebbles of 5-15 mm diameter and

rounded to subrounded fragment of mud. The Sp f a d e s i s

often succeeded by cosets of la rge scale trough crossbed

(Fig. 4A; and Fig. 3 Trench No. 1 ,2 ,3) .

Trough Cross Bedded Facies (St)

The large sca le trough corss-bedded facies occurs

interbedded with p lanar cross bedded ( Sp ) facies , spec ia l ly

in point bars , a t Shergarh, Mahavan and Agra. This fac ies i s

grey and d i r t y white in colour and occurs in cosets and

l o c a l l y in s ingle s e t s (Fig. 5 A / B ) . Individual forese ts

are s t r a i g h t to cu rv i l i nea r and tangent ia l a t base and

tnincated a t top in a-c sect ion, and trough l i k e in b-c

sect ion and are on an average 5 cm to 75 cm th ick . In most

trenches fores t angle to gent le (10*). The scale or thickness

of cross bedding i s about 30-50 cm or more near the

Fig. 4A : photogrqph showing cosets and sets of cross-

bedded sandy fades (sp) In vertical section

showing a progressive decrease in scale of

forset from base to top.

Fig, 4B : Photograph of planar cross bedded sandy fades

(Sp) in the lower part of point-bar cycle.

FiG. kA

FI6. kB

Sector-I Nouhjnil o.

c SHERGARH

0 5 o 0.5 Km

Fig. 3 : Map showing the general course of the

Yamuna river at Shergarh, (Sector 1) of

Mathura district, niack dots In vertical

sections indicate location of trenches.

Fig. 5A : Photograph showing large scale trough cross-

bedded sand facies (St) in the lower part

and progressively decrease in scale from

base to top.

Fig. 5B ; Photograph showing large scale trough

cross bedded sand facies (St) .

FICi. 5"A

FI6.5B

'6

base of each cycle of the poin t bar sequence decreases

gradually to 10-20 cm in upward direct ion (Pig. 6) . The

mean thickness of se t s decreases v e r t i c a l l y from 78 to 10

cm from base to top of sequence in most of the t renches.

Trough cross-bedded se t s in channel bodies are gent ly sigmodal,

and loca l ly convoluted due to soft sediment deformation. In

channel sand bodies of t h i s facies/ the overlying and

underlying surfaces are eros ional . Good sect ions of th i s

facies are seen in trench no. 1,2 of Fig. 3) .

Large scale St facies i s succeeded upward gradually by

small scale St f a c i e s . The lower un i t of t h i s facies may be

deposited by migration of la rge dunes as the ve loc i ty of

flow of water decreases . Likewise, grain s ize decreases

upward in each point bar cyc le .

Mode of Formation

The avai lable l i t e r a t u r e on recent and ancient sediment

suggests, t h a t cross-bedding i s formed by various ways. There

i s a general agreement annong sedimentologists t h a t the

formation of cross-bedding i s control led by cur ren t velocity,

flow c h a r a c t e r i s t i c s , and the kind and r a t e of sediment

supply. The cross-bedding of large scale ( > 5 cm in thickness),

spec ia l ly when they occur in cosets , aire formed by the down

Fig. 6 : Photograph showing small scale trough

cross bedded, sand/sil-fi fades (Sr) in

the upper part of the point bar sequence.

Fig, 7 : Photograph showing horizontal laminated

sand facies (Sh) overlying this Sh-facies

is Sm-facies.

Fig. 8 : Photograph showing inclined horizontally

laminated sandy facies (Sh).

F»^.6

FIG,.7

Fl^.8

1

stream current migration of asymmetrical mega ripples, dunes,

sandwaves (sorbay; 1859, iMeckee;19 57, Allen; 1962, 1963;

Jopling, 1963) .

Planar cross-bedding r" Allen (1963) concluded that

CO sets of p lanar cross-beds are formed from asymmetrical

r ipp les having s t r a i g h t and pa ra l l e l c r e s t s and the scale

of s t r a t a i s governed by the aii5)litude of the r ipp les .

According to Harms e t al (1982), planar corss-bedding may

have been deposited by migrating two dimensional large

r ipples . The occurrence of planar configuration of laminae

may ind ica te lower ve loc i ty .

The formation of planar cross-bedding suggests that

they are formed of sand by the logi tudina l and transverse

bars on the avalanche l e e side face. Upstream slopes (stoss

side) of these ba rs are gentler , and the sand migrating on

in slopes of l a rge scale r ipp les , s l i p s down on the steeper

slope (down cxirrent) or avalanche face following i t s

topography and produces large scale planar cross-bedding

(Sp - facies) . However, the small scale Sr f a d e s was

produced by the migration of small scale asymmetrical r ipples

having s t r a i g h t and pa r a l l e l onset and an^jlitude of less than

5 cm (Allen 1963).

1

stream current migration of asymmetrical mega ripples, dunes,

sandwaves (sorbay; 1859, Meckee;19 57, Allen; 1962, 1963;

Jopling, 1963) .

Planar cross-bedding r" Allen (1963) concluded that

CO sets of p lanar cross-beds are formed from asymmetrical

r ipp les having s t r a i g h t and pa ra l l e l c r e s t s and the scale

of s t r a t a i s governed by the airplitude of the r ipp les .

According to Harms e t al (1982), planar corss-bedding may

have been deposited by migrating two dimensional large

r ipples . The occurrence of planar configuration of laminae

may ind ica te lower ve loc i ty .

The formation of planar cross-bedding suggests that

they are formed of sand by the log i tudina l and transverse

bars on the avalanche l e e side face. Upstream slopes (stoss

side) of these ba r s are gentler , and the sand migrating on

in slopes of l a rge scale r ipp les , s l i p s down on the steeper

slope (down current) or avalanche face following i t s

topography and produces large scale planar cross-bedding

(Sp - facies) . However, the small scale Sr f a d e s was

produced by the migration of small scale asymmetrical r ipples

having s t r a i g h t and pa ra l l e l onset and anpli tude of less than

5 cm (Allen 1963) .

20

Trough cross-bedding • " Knight (1929), Lahee (1952)/ and

Meckee (1957) suggested t h a t channel and f i l l i n g are respon­

s i b l e for the formation of the trough cross-bedding. However^

the t ranqui l flow ra the r than shooting flow, siraon and

Richardson (1961) were of the opinion t h a t t h i s s t ructure

developes in the upper p a r t of the lower flow regime. Frazier

and Osanic (1961) have suggested t h a t the scouring of troughs

i s caused by eddies a t the advancing front of the sand waves.

(Allen 1963) concluded tha t small and l a rge scale trough

cross-bedding develope from the forward migration of the

l inguoid and lunate asymmetrical r i p p l e s . According to Aario

(1971) each trough f i l l i n g was due to down stream migration

of r i p p l e s . Trough cross-badding i s formed by the migration

of three dimensional la rge r i pp l e s (dunes and maga ripples)

(Harms e t al / 1982) .

In the developmait of l a rge scale trough cross-bedded

u n i t scouring occured when the ve loc i ty of current was high,

and was f i l l e d as there was a decrease in the current ve loc i ty

(Fielding 1986).

Massive to Horizontal bedded F a d e s (5m-3h) ~

Massive to horizontal bedded (Sra-3h) sandy facies are

grouped together because of t h e i r close assoc ia t ion . Massive

2x

sand facies (Sra) i s grey in colouir and fine to very fine

grained, l o c a l l y i t displays thin sandy l e n t i c l e s (2-4 cm

thick) and lacks v i s i b l e s t r a t i f i c a t i o n . Horizontal bedded

facies (fig« 7) may show inc l ina t ion l e s s than 5 degrees

( f i g . 8) . Generally, i t s thickness increases l a t e r a l l y away

from the bank (10-25 cm or so) , The hor izonta l laminated

facies (sh) i s white to grey in colour, and medium to fine

grained. These sheet l i k e bodies (10-40 cm thick) extend

l a t e r a l l y for a few tens of meters. Individual beds are

general ly equal to subequal in thickness and l o c a l l y contain

l e n t i c u l a r bedding. This Sh facies displays mica flakes

along i t s laminae and a t places shows angular to subangxilar

granules of quar tz and fe ldspar . In some trenches (nos. 1,2,5)

a t Shergarh and Agra, Sh facies i s overlain and underlain

by s i l t laminae having thickness of 0,5-2 cm. The bedding

surfaces are genera l ly devoid of r ipp le marks, indicat ing

deposit ion by r e l a t i v e l y high ve loc i ty c\irrent of upper flow

regime. This fac ies i s well documented in trench 5 a t

Agra, (Fig. 9 ) .

Node of formatioa

Massive or horizontal bedding may be in te rp re ted as

an in t e rna l s t ruc tu re of longi tudinal sandy bars (Smith,

1970), poss ib ly indi.cating t ranspor ta t ion in planar sheets

Sector.3

22

A G R A 0

• • • • ' . • - • . - • - __

I 1

TAJ MAHAL 0-5 0 0.5 I I I

Km F i g . 9 Map showing the general course of the

Yamuna river at Agra (Sector-3). Black

dots In vertical sections Indicate the

location of trenches.

7 *

under very high energy conditions (Rust, 1972b), Their

deposition may be a t t r i b u t e d to an increase in flow regime

due to local shallowing of the basin floor, seasonal increase

in discharge, or to sheet l i k e floods (Meckee e t a l . , 1967).

Bridge (1978a) described the or igin of horizontal bedding

under turbulant boxindary l a y e r s . The formation of horizontal

laminated fac ies can also take place under two qu i te different

conditions, in shallow water and flood stage (Harms and

?ahnestock 1965) , However, t h in ly bedded nature of t h i s

s t ructure suggests tha t these are formed under low energy

condit ion.

Channel F i l l Facies (Sch)

The channel facies i s seen in trench no, 1, (Fig, 9 ) .

The channel f i l l facies i s a convex sand body pinching out

l a t e r a l l y for about 3-7 m and in the down stream direct ion

and lens shaped in b-c sect ion, measured upto a length of

3 m and depth of 78 cm. Large scale trough cross-bedding

i s the dominant sedimentary s t ruc tu re occurring mostly in

the lower p a r t of the channel (Fig. 10) . The contact of

the channel fac ies with the underlying fac ies (clay/mud)

i s erosional but with the overlying fac ies , i t shows a

F i g . 10 : Photograph showing channel-f i l l ,cross-bedded

poin t bar deposit of the Yarmana r ive r , a t

Agra, On the top of the channel^the l a s t

phase i s seen f i l l e d with layers conforming to

the shape of the channel.

F i g . 11 : Photograph showing r ipp le d r i f t c ross -

laminated f a d e s (Sr) in fine to very

fine sand and s i l t .

F ig . 12 : Photograph showing s t ruc tu re l e s s massive

TAud (nYi\ ) in the middle pa r t of the

photograph.

FIG,.)0

^\C,.\\

^\(\.\1

7.^

gradat ional contact a t most p l ace s . The channel i s f i l l e d by

sandy l aye r s conforming approximately to the channel shape

with an upward concavity. The sediment of the channel f i l l

i s medium to f ine grained and d i f f e r s from the surrounding

sediments i n vAiich the channel occurs . The erosional hasal

contact contains pebbles of in xinderlying mud, arranged

along the fo r se t s of l a rge scale trough cross-bedding. The

pebbles of mud are over la in by nediura to f ine grained sands

showing small scale trough cross-bedding. Medium to fine

grained sands are followed by fine s a n d / s i l t showing p a r a l l e l

laminat ions .

Mode of Formation

Water flowing over a soft sediment surface under cer ta in

condit ions, erodes a channel (Reineck and Singh 1980), According

to Meckee (1975a), channels are produced e i the r by streams in

pa r t l y subaer ia l pos i t ion or by submerged (or submarine)

c u r r e n t s , scouring may develop, by the action of eddies and

such hollows p e r s i s t long enough to be observed during low

water s tage . Laminations p a r a l l e l to the lower bounding

surface, suggest formation under submerged conditions

(Reineck and Singh 1980) , xhe occurrence of large scale

trough cross-bedding suggests t h a t the scouring was done by

J

e d d i e s a c t i o n when the v e l o c i t y of t h e ciorrent was h igh;

i n - f i l l i n g of scour took p l a c e wi th dec rease i n cxorrent

v e l o c i t y .

FINS SAND> SILT & CLAY FACISS

Ripp le lanainated t o Ripp le d r i f t l andna t ed F a c i e s (sr) 7"

The 3 r - f a c i e s c o n s i s t i n g of fine sand and s i l t showing

small scale c r o s s - 1 ami n a t i o n i s well exposed on the

concave s i d e of r i v e r bank i n t h e upper p a r t of p o i n t ba r

sequence as we l l as on the convex s i d e i^Jlrloe-dAjLcL with

l evee sequence (F ig . 11) . I t i s a l s o found t o be p r e s e n t in

subsur face s e c t i o n s . The observed t h i c k n e s s ranges from 20

t o 150 a n . The r i p p l e c r o s s l amina t i on may be trough, p l ana r

o r type A and type B r i p p l e d r i f t l amina t ions o r g rada t ion

between them a f t e r J o p l i n g and Walker (1968) . The amplitude

of r i p p l e s i s l e s s than 1 cm.

When S r - f a c i e s i s t h i c k bedded, i t may be in t e r -bedded

with l amina ted sand and s i l t f a c i e s and i n d i v i d u a l u n i t s are

normal ly l e s s than 60 cm and c o n t a c t s between them are smooth

or s l i g h t l y u n d u l a t i n g with a r e l i e f of a few cm. At p l ace s

hoof marks of animals t r a i l o r marking of microfauna can be

r e c o g n i s e d . I n d i v i d u a l u n i t s may be d e p o s i t e d by low

26

frequency waning flood.

Interpretation

Bucher (1919)/ Renieck (1963b) and ifeckee (1965) have

observed tha t the r ipp le d r i f t cross laminations are

developed where the excess suspended sediment i s continuously

avai lable to a current or wave* vAiich i s i n turn deposited

above the e a r l i e r formed r ipp led l aye r . Field observations

reveal tha t the r ipp le lamination in d r i f t and in phase both

are developed simultaneously. A s l i g h t change in depth of

flow, supply of sediments and in ve loc i ty of current resu l t

in the d i f f e ren t arrangement of c r e s t of the r ippled layer .

The continuous supply of the sediment helps in the formation

of r ipp les in sand which migrate continuously without making

any permanent s t r u c t u r e . The burried/suspended sand and

s i l t preserved may give r i s e a s e r i e s of superimposed r ipples

(Reineck and Singh, 19 8o), They may develop in pheise, i f

the ve loc i ty of the water i s l e s s and depth i s more or in

d r i f t , i f the ve loc i ty of the preva i l ing cur ren t i s s l i gh t ly

higher and depth i s l e s s (Kumar and Singh, 1978) .

Muddy F a d e s (Mro)

Muddy facies mainly con^rised of s i l t and clay and i s

Khaki to black i n colour (Fig . 12) . This facies i s Khaki

21

in colour and esdiibits r o o t l e t s and organic material vdth the

occurrence of the sand bed (15-50 cm thick) including s i l t

and c l ays . Muddy facies occupies the top portion of the bank

depos i t s and general ly lying above the sandy facies . The

thickness of muddy sequence i s upto 5 ra a t p laces ; i t extends

up to 7 ra thick in ve r t i ca l sequence. A number of sedimentary

s t ruc tu re has been observed in the muddy f a c i e s . Among the

sedimentary s t ruc tures are convolute bedding, r ipple d r i f t

c ross lamination and wavy laminat ion. The convalute bedding

occurs in the upper p a r t of the deposi ts vftiere the sediment

i s c lay or s i l t and individual u n i t s in which convolute i s

found ranges in thickness from 40 - 50 cm . The muddy

fac ies i s also character ised with a decrease in grain size

from the basal to the upper p a r t and generally occurs as

shee t - l i ke deposits v*iich may be trraced l a t e r a l l y for a

considerable distance (Fig. 13) .

Interpretation

The muddy facies may have been deposited by suspended

load a f te r the flood, and may be in te rpre ted as overbank

flood sediment. This fac ies may also be associated with

minor crevass gpiay deposi t , mud layers gives an idea about

the nuniser of flood episodes occured during the deposition .

of p a r t i c u l a r sedimentary u n i t .

Fig , 13 : Photograph showing thickening of muddy

f a d e s (Mm) towards levee deposit and

gradually thinning towards channel.

F ig . 14 : Photograph showing large scale trough

cross-bedding (in the lower part) and

convolute and cross d r i f t laminations in

s i l t (upper part) .

F ig . 16 : Photograph showing p a r a l l e l lamination

(SI) in the upper pa r t , in ve r t i ca l

sequence.

FlGv.\3

F1G,.\A

FlGv.\6

4S*r^

Ccmvolute Laminated F a d e s r" ^-^^^

The convolute lamination i n the f ie ld i s general ly

observed in fine sediments occupying the top por t ion i n the

bank depos i t s . I t i s genera l ly underlain or over la in by a

massive and undisturbed layer and sometimes shows an erosional

upper contact (Figs. 14, 15) . On the bas i s of the nature of

t h e i r axial planes they can be divided in to two types:

Type A and Type B.

Type A Type A convolute laminations are those in which the

an t i c l i ne s and troughs are both rounded, and axial p la re i s

v e r t i c a l . The an t ic l ine i s not so broad and rounded as the

trough. The thickness of the individual xinit of the

convolute lamination ranges from 8-20 cm. The individual

laminae shows large va r ia t ion and a l t e rna te with dark and

l i g h t e r coloured laminae.

Type B: In type B, the axial plane i s inc l ined dipping in

down current d i r ec t i on . The laminae have been folded

in t ense ly with no sign of f a u l t i n g . The troughs are broad

and rounded and the an t i c l i nes are sharp and poin ted . The

individual un i t of convolute lamination ranges from 8-30

cm in thickness and general ly over la in by a muddy layer or

by r ipp le d r i f t cross lamina t ion . (P ig . 11) .

}-0(

f rtt»vci\ l

4 km

N

^c.o

0.5

h-i-o

.1.5

jK •-^'•y•

\- l - o

F i g . 15 : Map showing t h e genera l flow of t h e

Yamuna r i v e r a t Mahavan (Sector 2) Black

Interpretation

The convolute lamination i s a con5>lex and polygene t i c

s t r u c t u r e . However/ i r r e s p e c t i v e of di f ferences in i n t e r ­

p re ta t ion and d ive r s i ty exhibi ted by the s t ruc tu re i t s e l f ,

i t appears t ha t the s t ruc tu re a r i s e s in response to a v e r t i c a l

pa t t e rn of pressure act ing upon p l a s t i c and laminated sediment

(Harws, 1982, Reineck and Singh, 1980i • Several explanations

have been proposed for the genesis of convolute lamination.

Kuenen (1953a) believed tha t convolute lamination developed

from the deformation of the r i p p l e marks. William (1960)

suggested tha t convolute bedding developed from the deformation

of the r ipp le marks. William (i960) suggested tha t convolute

bedding i s produced by d i f f e r e n t i a l l iquefac t ion of a

sediment u n i t . Lateral i n t r a s t r a t a l flow of these l iquef ied

u n i t s produces contor t ion . Mckee e t a l . (1962) and iickee and

Goldberg (1964) developed convolute bedding in laboratory by

placing d i f f e r en t i a l load from above and concluded tha t

ve r t i c a l forces r e su l t ing from overloading are important in

generation of convolute laminat ion. Hcvevec, Collinson

and Thomson (1982) regarded tha t the convolution involves

the p l a s t i c deformation of p a r t i a l l y l i que f i ed sediment soon

af te r deposi t ion. 3ut in the presen t area i t looks tha t i t

has bee.i developed by escape of water a f te r the deposit ion of

the sedirasnts, or by d i f f e r e n t i a l loading.

Parallel lamination ( s i )

Harms and Fahnestock (1965) described t h i s s t ructure as

s e t s of laminae in which individual lamination are p a r a l l e l

to the lower se t boundary. This s t r uc tu r e i s commonly

observed in fine sand, s i l t and c lay . The lamination show

a l t e rna t ing dark and l i g h t colour bends. The thickness of

laminae ranges from 2 cm. The laminations do not show

any kind of undxilations. This s txucture i s mostly observed

in overbank deposi ts bu t also in channel facies C *" " - '

Mode of Formation

Para l le l lamination are developed in f ine sand, s i l t

and clay. In f ine sand p a r a l l e l lamination i s formed vrtien

the flow ve loc i ty i s high and water depch i s shallow under

upper flow regime. When such condit ions e x i s t the r ipp le s

and dunes are destroyed. In such condit ions water surface

i s smooth l i k e glassy appearance (Collinson and Thomson,

1982) .

C2iAPTER - IV

GRAIN SIZE ANALYSIS

GENERAL COMMENTS

Grain s ize a t t r i bu t e s of sediments and sedimentary

rocks are important tools to understand the processes and

environment of deposi t ion. During l a s t few decades the

environment of deposition has been determined on the b a s i s

of grain s ize d i s t r ibu t ion (Folk and Ward, 19 57; Mason and

Folk, 1958; Harms, 1959; and Friendman, 1961, 1971). These

workers used the s t a t i s t i c a l parameters such as mean s i ze ,

standard deviation, skewness and ku r tos i s of f luvia l

environment. This approach has been moderately successful

p a r t i c u l a r l y in in te rp re t ing modem environmenTss. Grain

s i z e d i s t r ibu t ion are mixtures of two or more subpopul a t ions ,

produced by varying t ranspor t condit ions (Doeglas, 1946) .

ln.T.an (1949) dis t inguished three populat ions ( t r ac t i on ,

s a l t a t i o n , suspension) on the ba s i s of shape and s ize of

sediments. These processes were applied by Moss (1962, 1963)

using the shape and s ize of grain and d i s t ingu i sh subpopul a t ions

Moss (1963, p . 840) described tha t fine sediments

t ransported in suspension usua l ly have an upper size l i m i t

of about .07 to 0,1 inn. Sa l t a t ion have an upper size l i m i t

of about 25 to .17 mm and t r ac t i on have an upper

s i z e l i m i t .5 to .25 mm. Visher (1967, 1967b) observed in

recen t sediments t h a t most sedimentary laminae contain

gra in size of an order of .1 ran or smaller s ize f ract ion,

^*iich are d i r e c t l y deposited from the suspension mode of

t r anspor t .

GRAIN SIZE VARIATION

TO Study the ve r t i c a l and l a t e r a l va r i a t ion in grain

s i ze d i s t r i bu t ion , sediment samples were co l l ec ted from

trenches dug along the coxorse of Yamuna r i v e r from Shergarh

Mahavan, Agra and Etawah. The data of graiin size c lasses a t

i n t e r v a l s of 0.25 cm are l i s t e d in t ab les 1.

Cuimilative frequency c u r v ^ were p lo t t ed on log

p robab i l i t y following the method of Visher (1969). The

grain size d i s t r i bu t i on was grouped broadly in to three types

of p robab i l i t y p l o t t s mainly on the bas i s of number of

subpopulations and t h e i r percentage and so r t ing . The mean

s ize sediment ranges from 0.257 tc ,057 im. Out of 56

samples, 26 sanples are fine sand, 7 sarrples are very f ine

1 m M l f l

• • > * *

1 i n O CM

• •

t i n

t- o • • n *

• *

<J> 0 \

t-i

• Oi

o\

VO

• cu a\

a> a\ • o>

o>

<> • i n ON

o • ^ T-t

1

m ON

• a\ O l

o • o\

O l

1 1

0 0

1 a\ o\

NO

• 1 0\ c\

cu ON

n « rv)

Ol

o o o t

1

1

m • ON

ON

o> m ON

(t) • ON

ON

ON O l

n Ol

• O l O l

f S

• m Ol

o • VO

ON

I in in r-

I in Mm

I in O CNl

I m o r- o

I m

I m < N m

I m o fNi

m o r- o

I m m t~

I I I I

ON ON

03 O O

ON CO ON m

ON ON

• • r- r-

o) m ro CO lO NO

ON ON Ol ON ON ON

ON ON CO ON ON ON

CO O ON CO

NO CNl ON O

I ON fN CO NO

ON f n cNi CO o o

CD ON c^ ON

O CD ON o* 00

tN CO rH 00 ON m

*-* O N O N O i O O C ^ O N ^ O N

CO CTN r j fo

Ol ON ON ON

o o

CN) ON

CO O N c o t H m ^ m v o r - o i O N O N O N O N C O O N O N O N

CO NO lO m

O IN n ID m fo

GO ON r- lO c^ Ol ON ON

CO CO

ON

o

ON

•<f

r*y

ON

0 0

9 ON

l O

o o m

NO

ON O l

ON

f O

ON ON

O N

ON

CD

0 0 ON

O l

fNi

ON

l O

n

ON

O

o o 00

•<(•

00

o o m

c m o Ol ON ON CO CO

c^ Ol NO CO ON m m NO

m NO fNj ON C7N ON ON Ol 00 00

OO CO ON ON ON ON

o o o r^ m fNj o Tf m o ru <N o

o o •-•

CD ^ m CO CO CO lo r^

<N O O CNI

CD CD O ON CO ^

CO <n

CO m CM CO

m r ^ i o i c O N O c o r H O 0 N | t H » - i n r i i r ^ ^ c n ^ H i o m ' H t - * o O N v o f N i c ^ o i m ^ O N m r ^ O i r « v o m t N r o ^ r - [ ^ r - n v o o o ^ » - i ^ O O I O V O N O I * ) rH C O O O O N

CO o r ) o • * CNi CM rH m m ^ m m

( N o o o c o o m n m o O t i « ^ i j o i o o o T f o n • < j t o o f M

m NO o tM m

f o CJN ON r ^ m

m CM

00 N O c n o N o O N m c o o m n i m o O N * H r - m m

O CO •H CO

o CO CO cNi m

O NO

NO

r~ • * o

I m cNim

I o m O (N|

I m o r- o

I m m r »

I O m

I n u n u

H B 10

NO ^ m

N O I I O M I O C N l t N l | f - I C O

m -^ m (N m n m (^ r o n cjN fNi

O <N r~ O CM d NO O r H o c o N i f i n o o i f - i m l m c M i t t ^ m l m l m ot o

I I I O I O (O

r^ o CN) r ) NO 00 ON i i

rH r-t C>t

I I O CM ^ ON CNl I

m ^ n

I I CA NO NO I

NO m r^ CM m m o i l N O C N I I I I l O I I N O O O l O O O O m C M I I I I l l l l l l l l < N | | |

I I I -« I I I I I I I I Tji ^ ro »H »H

l « « l • • • l l l l l l l l l I I I I

I I I l l l l l l I I I I I > I l l l l l l l l l l l l I I I I I

C N i f o ^ m N O i H c M r ) ^ | f ( v D r - o o t H c M n - ^ r m N O r ^ . - i r M r o NH IN n ^

1

c dl Q - c .

m o St 3 - H

t o m

1

4J, C J « •=X 0

HJ-H CO i n 4J

1

<4) ' I D - H <<

m -P

< 0 c _ m o s< U -H H -P

4J

1 •K-

r>

o •p 14 n u 3 - H ^ i ^ m

+) • ^ • H t j

' m VI

v C H

> « 0) W

>: n

•p

•g • H

i J

1 1

C - H C „ 10 X I > O i T

t o 10 Q +J

*> - H

e • H i J

g) N

• H PI

c ;e 10 01

.X

E s

- e h

>M

n \ 3Z <U 4J «

S o u

(U 4J 0 <n 01 i i )

V r H

e-

j i n r-t

^ t H

m

( N • H

T - (

o •-(

o\

CO

r*

VD

i n

-*

r >

OJ

«H

•P 4J

o a

^ . u u (U 3

01 n a ti o 1) » u a a +J •H > i CO IJM 0 ]

4J

> X

;^

Si

•^ "S.

n H) » T 3

i X 4 J

u u 0) O

> n

CO i n »H

• TJ

c 10 n u c

• H PM

s

o >o • H

•

I) n U 4J

Sc3 U 01

•

r^

• "D

10 W

<D

•H PH

(0 u c m u

> ! • » - ,

i J +J 10 U

^ 3 a , M

f-t O *J

n u V 3

2 i ;

>,-,< JJ +J 10 V4

M 3 11. X

0) 3

^ •a c

•H 'O •D C 0) (0 X m

a) c •rt t .

i j

3 o u

in

u o -

•p +j a ij 0) D

rH n

•D 01

ID * B H)

•H A ;

t>4 in

• a (U

ID > C 0)

•rt > ; b t m

•D 01

(1) J C 01

• ^ X fr* in

• o (U

HI J c <u

•H ^ &1 in

X I lU

01 S C (U

• H X

&. «

•D Q)

<D S c H)

• H J i t . in

H . H 01 : » • o

m s^p M i4 01 O

> w

X )

5 u o 10

5 01

3

•-t H 0) X I 3 01

•P > . U

u o 0) in

>

•D

p i<

o n

- H --H 0) 2

X !

2 L( 0

m M -H (1»

^ ' O

OJ t l •P 0 ro in u 0) r-i

v^ O ill

s s

to 10

t-i (N

CD 00 ^ t-i cn lo

I IT) »H

u O -H JJ p

0) 3 !S 0) 3

O -P in U

5" H

O -P n 01

s r i O)

U 3 J<

j 3 fli 01

P l< 3

>J ^

r> ON r-*

- H 01 13 :» i)

V

>^u u o 01 in

>

M O in

M f H 01

S

H r-i 0)

» -o 01

t ^ p

u u 0) O > CI

• n 01 p M

o in

M r H 91

3

x> > i Q)

- H t J 01 Ui

4J 0 (0 in M «) H XJ r-i Q o;

i; 3

WXD

I I 10 > n

•P Q< lilt E O* O* 10 10 in i la 10

rH CM m

c o u

i n

in U

2: X

t) 01 ? 0)

>: U]

0 c

•a (U ; j 0) x 01

0) c

+

3

m r-

c ID W

0) C

O ON

(u a

•o c M

01

c

c in p> (0 x; ID

o

in u

"5

CD CO

c 10 n (U

•ri

in CO

u 0 -r l

at 0) 3 J .-<

u i>t -H

M ID Ul : <D ^ ;3

> a.'^

0 0 -H

a n m 3 ^1 v;

1

1 > > -ui^ ID P a)>, z w

•d di 1

in

0)

c • H CM

01 3 X)

W

&t 0) 0 > w

•a (1)

ti 0 in

0) . 1 ^

i c ^ r-t

0) 15

> i I j

'd <u f, 0 tf)

-H '-t

> i ' 0

r-o

o > . - H

(D M r-i a I I , X

•a <u \i

>^ 11) .-1 .v; U> "1

d 11) 1) c; JJ -rK u) HI

•d 0) 3; 0)

• ^

n u c: • C'-*

•a 0) }E 0)

,y in

D C

• H ! • !

1 - C

^ • ^

. 1

(.)> d i j

u '/-)

0) y. X)

11)

U'ti 11) 0 > 10

0

> u Q)

>

T3 C m in

0)

c •H

0) c

• H 1 «

&? ID (0

o 0^

ID U O • : i

O) <

.c u

O CO o\ in

O 4J in U ••

X) <u :* a) .y U)

0) : C

- H C>.

• d 0)

''\ > i 01 - s ,v; 01 in C 0 0) u n JJ .H 1.) IM

0) :s d

0) ; i 4J =

11) O

> w

0)

,-1

0)

(NJ 00

U

0) 3

IN

"-J

ir ^ M - 10 B : OJ S SB 1/1

0) 3

(!) .i1 i n

4)

t . i

+

(N r~ O CO

&1 0) la

o 'A

o CO

o > 1 - r <

13 U M 'J i i , :A

o U3 03

" • a (U V

OJ M 10

OJ a TH

fn

U T 4

0 U

0) -J : • ; • ' • '

o o • r H

'O QJ

ti o CO

r ^

H 0) 3:

03 > i 0)

0) t i »> O 10 W M 0) rH

' 0 rH 0 V

2 3

CTv

• u G to 10

0) a

•H c

• d -

i n

01 C

-H 4-1

> t ' a M 0)

>

VO O

c fO en

0)

Q) O > in

c

(0

0)

^ ^ o in

o Lf)

'O a)

Ul

01 c

(;

'1 ^§ U f 0) i>i •A w

o o

OJ s

> i (U

a O 0) l-i C -(J -M

ro cr> r-

r-a

0

^ j : : (J

r o CM

t

r-4

j _ )

00 O

• rN

j j

00 O

• CM

1 1

u O -rK

atl aj ;) , 1 .'•'

o

^

u •rH

O i J m U 0) 3

• ' • • ' • '

CT. o

-

^ o

o O-rA

P,ti (U p . 1 ;^

t -•>3'

+

(U

o ID

Oi rH

ro

• ^

• *

ro

CTi • *

ro

r-CTl

•"a"

t-l

> i ' a

M G

> m

o

GgMN SIZg DISTRIBUTIOH IN RELATION TO SEDIMENTARY STRUCTURES

Planar Cross-bedding Sand Facies (sp)

Planar cross-bedded sand fac ies was analysed for grain

s i ze a t S her gar h, v*iere t h i s f ac i e s i s well developed. Six

samples were analysed (Table 2, and da ta were p lo t t ed on

p r o b a b i l i t y paper as shown in F ig . 17 a, b^ c, trench No. 1,2,

3) . The bxilk of each sarrple from Sp fac ies cons i s t s of two

sxobpopulations of s a l t a t i o n load (Sa l ta t ion A and Sa l t a t i on 3 ) ,

a phenomenon also recognised e l se v^ere by other workers

(Moss, 1963; Visher, 1969; Quidwai and Gasshyap, 1978) . Some

samples include a va r i ab le admixture of t r ac t ion and suspension

load . Sediment s ize corresponding to i n f l e c t i o n poin ts a t

coarser end, between t r a c t i on and s a l t a t i o n A/ ranges from

1.0 0 - 2.0 0 (.50 - .25 nro) and for those a t f ine r

end, between s a l t a t i on B and suspension, from 3.0 0 to 3.5 0

(.125 - ,088 ran). In f lec t ion po in t s between s a l t a t i o n A

and sa l t a t ion 3 siibpopulation range from 2,5 0 to 3.0 0

(.177 - .125 rrm) .

I t may be inferred t h a t the sediment load of Sp f a c i e s

has been transported l a r g e l y through s a l t a t i o n load which

cons t i t u t e s about 75 to 98 percent by weight of the sanple ;

suspension fract ion va r i e s from 5.5 to 18.8 percent , whereas

ioor~

9 5

•—

z UJ

UJ Q.

t— x o

8 A

7 5

50

7.5

t i l 16

3

u

LA

UJ

2.

U

< o 1/)

T r e n c h - 1

- U J-. _!. J - -I 0.5 IX) 1.6 ^;5 2:5 3 ^ 3.5 /.X) ^'.5 (f

1.0 0.5 0'35 0 . 2 5 0.177 0-125 0-088 0.05Z5 CJ.O/:, i^imm

F i g . 17 a : Diagrams showing Log p r o b a b i l i t y p l o t s of

gra in s i z e d i s t r i b u t i o n of Trench No. 1 :

-o- ^

11 s

-J o

L N i j b j d 1 KO Id M 3AI1V i n n n J

ta t i lM »t i w l t

ifrj3'M3<i in'oi3M "aAilvinwriO

KV

-J

3

i n

«

F:' [:

J -JT Cl

o in «s

6 t/t H

O o

O

i n

6

b o

>n 9 • o •^

iO

t r ac t ion load, as and where present , conprises aix>ut 16

percent . Evidently/ the bulk of the sedinent of t h i s fac ies

was deposited under condi t ions of lower flow regime.

Overall , the sand depos i t s of Sp facies have a mean s ize

ranging from 2.26 0 to 2.60 0 (.209 - ,158 irni) with standard

deviat ion ( ©— i ) .523 0 t o . 2,62 0 suggesting t h a t the

sediment i s very well to moderately sorted; skewness (SKI)

ranges from +0.0 to +0.264 ( f ine skewed) and kur tos i s (KG)

from ,573 to 1.97 (very p la tykur t i c ) to l ep tokur t i c ) ,

(Pig . 18 a,b,c)

Computed average of the s t a t i s t i c a l a t t r i b u t e s for s i x

sanples showsthat the p lanar cross-bedded fac ies , by and

l a r g e , cons is t s of f ine sand (r-L ; 2.45 0 0.183 mm); i t i s

very well sorted (®- I : 0.394 0 ) , fine skewed (SKI: +0.168),

and l ep tokur t i c (KG: 1.15) .

Large Scale Trough Cross-bedding Sand Fades (3t)

The cumulative p r o b a b i l i t y p l o t s of sand fac ies with

l a r g e scale trough cross-bedding for grain s ize analysis of

s i x sanples (Table 2) along the course of r i v e r co l l ec ted

a t Shergarh, Mahavan and Agra show in t e r s ec t i ng p lo t s with

one or two inf lec t ion po in t s (Fig 17-bc, 19, 20-c) . The f i r s t

0.0 r

UJ

1.0

3 Sh

2 Mm

T r e n c h - 1 FIG. 1 ^ C

0.0

ac UJ I— U)

S

5 1.0

UJ

< U1

, 2.0

3 Mm

7 St (Large scale)

1 I L_

FIG I g ' • b

0.0

(X

UJ 3

Z 1.0

2.0

_i_t 1 I _j i_j I I

r r e n c h - 3 O O 2 •» 6 0 O O ,2 .4 .6<t> - 4 - 2 O *1 <• * • . « 0 O I 2 3 <fc

-1 ! m m OO 0.25 .0625 .015

Mean S ize

Mz

f'(- IS a S.Dev ia t ion S k e w n e s s

S K I K<jr tos is

KG

Fig. 18 : Size frequency cumulative percent plots

of Trench No. 1-3 at Shergarh. Vertical

' • ^Qf

N

^ \ "*" e

l\^o s" V-b^

\ v \ • ^ • ^ \

\ i \ \ \ ^

\ X-* -D \ ^ ^ V*\^

v= ^ N

_ >" o

JNBO' tOd . I H 9 I 3 M 3 A l i V i n w n O

So]!!!-* Ni 3"v35

o

a

o - I o LI

J L

0 LI a 1 o> 0

. J

0> c J 0

n E « u CT fl

c 0

:i 3

XI •rt

iJ 0)

•H •o

0)

•H to

c •rt 10

. c ID

> HI x:

1 N 3 3 M l r i l u o i ^ M 3AI1 » i nu ,n>

9 95 9

21

UJ

UJ

a I— X o uJ UJ

>

95

7 5

5 0

25

16

I I I JL I J_ 0.5

\0

1.0

0 . 5

1.5

035 2.0

0 . 2 5 2.5 O.I?5

3.0

0 .088

J 3.5 ^.0 A.5 ({)

0.0625 0 .QB8 o.oUM Y A V n

F i g . 20 a : Diagrams (a, b, c,) showing Log-probabi l i ty

p l o t s of grain s i ze d i s t r i b u t i o n of Trench

5-7 a t Agra.

9 9 9 9 r

A.O. ^..5 ()

0O63.S O . o M t f m m .

99yy

95

84

75

o Qt: 5 0 UJ

a

O 25 UJ

^ 16 aJ >

Z3

0.5

1 0

JL IX) 1.5 2.0

0.5 0 . 3 5 0.25

JL 1 _L 2.5

0.177

_L _L 0- J 3.0 3,5 4 0 /.,5 ,p

0-12 5 O.OSB 0 -0625 DOUi-i -VT\ T

i n f l ec t ion point between t r a c t i on and s a l t a t i o n ranges from

1.0 0 to 2.0 0 ( 0 , 5 - 0.25 mm), and second l i e s between

3.0 0 - 3.5 0 (0.125 - .088 rrra) , The bulk of sediment

load cons i s t s of t r ac t ion (6-18 percent) and s a l t a t i o n

(70 - 90 percent) and s a l t a t i o n (70 - 90 percent) load;

suspension load ocoxxrs in subordinate type ( lOji) .

Overall/ the sand i s medium to fine grained with mean

s ize (Mz) ranging from 2.16 0 to 2.616 0 (.224 - .167 mm),

and very well sorted ( o— I ; .271 to ,28 0) . Skewness

and ku r to s i s values show t h a t the sediment i s fine (SKI :

+ .118) to strongly fine skewed (SKI + .454), and p l a tykur t i c

(KG t .705) to l ep tokur t i c {YiG : 1.36) a t Shergarh (Fig. 18,

3/ b ) .

For St facies a t Agra, the sand deposi t i s medium to

f ine grained with Mz : 2.08 0 to 3.08 0 (.213 - .336 mm);

very well sorted (<^ I : 0,318 - 0.349 0) f ine skewed

(SICj. : + 0.003 to 0.0793) and lepto to mesokurtic (KG : 1,04 tc

1,40) (Fig - 21) .

The computed average of s ix sa»'T55les of trough cross-bedded

sand facies shows tha t the sandy facies coraprisses of f ine

sand (Mz : .183 ima) ; i t i s well sor ted ( cr- ; 0,394 0) f ine

.oL

U S t I S m a l l s c o U )

S m - S h With mud P'b6(ts

/

1 St (Smal l seals) „ / _ _ j 1 1 -

b

^ St (Small scQte)

St ( Large scolf ) with mud pebbifs

oo a * •0 OO O i 5 0635 CMS

Mean Sue

MZ

OO a * » (

S Otv iot ion

T

- 2 O - 2 . 4 - 6 . . . 9 0

S V f w n n s SKI

CL

O I 2 ]

Kurtos is KG

Fig. 21 :' Size frequency cumulative percent plots of

Trench No. 5-7 at Ag^a. Vertical sections

(left side) show generalise facies model.

skewed (SKI : + 0.168); and l ep to kur t i c (KG : 1.15).

Small Scale Trougl>-Cross bedding (sr)

Probabl i ty p l o t s of s ix sanples of Sr facies exhib i t s

three sediment populations (Fig 20 a^b) . This facies i s well

developed in trenches and e^sposed sect ions a t Shergarh and

Agra (Figs. 17-b,d, 19a, 20 - a ,b ,c) .

Sediment s ize of in f l ec t ion po in t s between-traction and

s a l t a t i o n A ranges from 0.5 0 to 2 0 (Q.71 to 0.25 nan) and

for those a t f iner end between s a l t a t i o n B and suspension

from 0.3 to 3,5 0 (.125 - .038 mm), i n f l ec t i on points

between sa l t a t ion A and s a l t a t i on B subpopulations range

from 2 0 to 3 0 (0.25 to 0.125 rrni) . In each fac ies ,

s a l t a t i o n population cons t i t u t e s about 63-96% of t o t a l sample,

suspension loads from 4 to 35;^, with a few exceptions/ t r a c t i o n

load includes 2-6 percent of totcJ. sanple load .

This facies i s ccxisists mostly of very fine grained sand

v/ith mean s ize (Mz) varying from 2,25 0 to 2,9 0 (.210 - ,154 ma);

very well to well sorted (JT" l = 0.374 to 0,479) . I t i s f ine

skewed (SKI = + .106 to + 0,190) and commonly mesokurtic

(KG = 1.04 to 1,092) a t Shergarh, north of Mathura (Fig. 18 .) ,

The small sca le trough cross bedded sand facies a t

Agra i s very fine grained (l-Iz : 0.210 -0.154 mm), well sor ted

(cr~ I = 0.399 to 0.497 0 ) ; i t i s s t rongly f ine skewed (SKI

+ .071 to + .476) and comnaonly leptokxirt ic (K3 : 0.860) to

p l a t y k u r t i c (KG : 1.47) (Fig. 21 a ,b^c ) .

Average of Hie s ix samples shows t h a t small scale trough

cross bedded facies, by and l a rge , cons i t s of very f ine sand

(Mz) 2.746 0 (.181 mm) which i s well sor ted (o^ I : 0.434 0),

f ine skewed (SKI: + 0.181) and commonly lepto)curtlk

(KG : 1.128) .

Horizontal Laminated Sand Facies (Sh)

Like\idse five sanples of hor izonta l laminated sand fac ies

(Table 2), graphic p lo t s of cumal a t ive weight percentage

(Figs 17 a-b, 20 a) y ie ld three sediment populations of t r a c t i o z ,

s a l t a t i o n , suspension along the covirse of r i v e r a t Shergarh,

and Agra. Sa l t a t i on population cons t i t u t e s about 30 to 90

pe rcen t (by weight), suspension sediment from 30-26%, whereas

the t r a c t i on i s less than 10 pe rcen t . However, in each

sanple s a l t a t i o n load cons i s t s of two subpopulations ( s a l t a t i o n

A and s a l t a t i o n B) . The sediment s ize a t in f lec t ion p o i n t

a t coarser end, between t r ac t i on and s a l t a t i o n A, ranges from

1.0 0 to 2.0 0 (0 .5 - 0,25 mm) and for those a t f iner end*

between sa l t a t ion B and suspension, from 2.5 0 to 3,5 0 .

In f lec t ion points between sa l t a t i on A and sa l t a t ion B

sxibpopulation range from 2.5 0 to 3.0 0 (0.177 - 0.125 ran).

The facies i s f ine grained with mean s ize (Mz) varying

from 2.35 ^ to 2.9 0 (0.133 - 0.196 mm), well sorted

( c ^ .452) to poorly sorted i'^'^ 1.56 0) j s trongly f ine

skewed (SKI : + .30 to +.427) and commonly lep tokur t ic

(KG : 1.12 to 1.17) a t shergarh. (Fig. 18 b , c ) .

The average mean s ize , standard devia t ion, skewness,

kur tos i s va r ies from shergarh to Agra in the facies i s f ine

sand (>S J 0.172 mm), which i s well sor ted (o~-I = 0.376 0),

s t rongly fine skewed (SKI : + 0.3 22) and mesokurtic

(KG : 1.107) .

Ripple Cross dr i f t laiainated Facies (sr)

Cress d r i f t laminated fine sand and s i l t facies was

analysed for grain s ize a t Shergarh, Mahavan and Agra. Four

samples were analysed (Table 2) and data were p lo t t ed on

p robab i l i ty paper as shown i n ( F i g . 17 be, 18b, 20 ab) . The

bulk of the san^iles from s r facies cons i s t s of two svib-

populations of s a l t a t i o n load ( s a l t a t i o n A and s a l t a t i o n 3 ) ,

some samples contain var iable admixture of t rac t ion and

suspension load. Sediment s ize corresponding to i n f l e c t i on

po in t s between t r ac t ion and s a l t a t i o n A, ranges from 0.50 -

0.25 rrin.and for those a t f iner end between s ta t ion 3 and

suspension from 0.125 - 0.105 ratii. Inf lec t ion po in t s

between sa l t a t ion A and s a l t a t i o n B from 0.149 - 0.053 nm,

I t i s inferred tha t sediment load was transported l a r g e l y as

s a l t a t i o n load which c o n s t i t u t e s 65 to 15% by weight of the

sample, with suspension and t r a c t i o n load

varying from 17 to 33? ; in some sanple shows the 83%

suspension load and t r ac t ion load comprises about 1.9%.

The bulk of sand i s fine to very fine grained with mean

s i z e (Mz) ranging from 0.148 - 0.135 rmi; i t i s moderately well

sor ted (cr-i :.150 0), s t rongly f ine skewed (SKI : 0.10 to

.303)/ and mesokurtic ij<C : 1.345) a t Shergarh (Fig. 18, ab) .

For t h i s facies a t Mahavan, the sand i s very f ine gra ined

to coarse s i l t (l-Iz: .134 rm); well sorted (o—I ; 0.434 0),

s t rongly fine skewed (SKlj ,143), and very p l a tyku r t i c

(KG I 1.1) (Fig. 22) .

At Agra t h i s facies i s f ine to very fine grained (Mz ;

,165 to .106 rrm), very poorly sor ted {9*^ I : 0.402 0) to

9 • *

(N - ^ O O

©•

o

o If)

€>i

C N O 2

O

n

O

a

c V o u

> • H +J <t5 i H 3

O

0) N •H

CM

•H

C o

U

m

n) O

>

c %

s o c 0) a D' 0) u >w

+j (0

-"t

0

o z J= u c

El

0)

(0

o M-l

(1) to

m M 0) c (U

w

o

w

1_

o d Sa3i3vN Nl 31V0S

ex t r eme ly p o o r l y worted ( I : 0.585 0) 7 f i n e skewed (SXI; +.251)

and l e p t o k u r t i c (KG : 1,35) t o mesokur t ic (KG 1.00)

( F i g . 21 b / c ) .

VERTICAL VARIATION IN GRAIN SIZE

F i g . 18 a, b / c demons t ra tes t h e v e r t i c a l v a r i a t i o n i n

g r a i n s i z e c h a r a c t e r i s t i c s a t v a r i o u s upstream and downstream

l o c a l i t i e s along the course of r i v e r Yanxina. As per p l o t s

of t r e n c h No. 2 ( F i g . 18 b) a t Shargarh , about 2.4 meters in

dep th , mean sediment s i z e d e c r e a s e s upward from .257 mm t o

.06 2 mm i n the lower h a l f ( sanp le 1-3) and .196 to 0.148 mm

i n t h e upper h a l f ( fo r samples 4 - 6 ) , i n d i c a t i n g t h a t the

given t r ench i s made up of two c y c l e of sediments ranging

i n t h i c k n e s s from 1.25 to 1.50 m, r e s p e c t i v e l y .

By and l a r g e , the g r a i n s i z e pa ramete r s do not e x h i b i t

a d e f i n i t e o r r e g u l a r v e r t i c a l v a r i a t i o n i n most t r e n c h e s .

However, t h e r e i s a tendency of rasan s i z e to decrease

s l i g h t l y from lower to upper p a r t of each c y c l e . Loca l ly ,

though, v e r t i c a l v a r i a t i o n i n mean s i z e or s o r t i n g i s well .

expressed e g . i n s e c t o r I , t r e n c h 2 a t Sherga rh . In t h i s

t r e n c h , compris ing some 1 - 2 ,5 ra of sediment , nean g r a i n

s i z e d e c r e a s e s for .257 to .062 rara. F u r t h e r down stream a t

Mahavan and Agra, l i k e w i s e , the v e r t i c a l v a r i a t i o n i n g r a i n

size may or may not be well developed.

The sediment is often very well sorted (0.307 0) in

lower part to moderately well sorted (0,505 0) in upper part

(sair|)le No. 1-6; trench no 2) (Fig - 18b),

CHaPTSl - V

HEAVY MINERALS OF YAMUNA RIVER SAND

Heavy m i n e r a l s of v a r i o u s l o c a l i t i e s i n Yamuna r i v e r

sand a re , by and l a r g e , s i m i l a r from s h e r g a r h t o AgA^* Heavy

minera l s i n d i c a t e t h e co i rpos i t ion of provenance and abras ion

h i s t o r y of sediments ( P e t t i j o h n e t a l . , 1972 s B l a t t , 1982) .

The o b j e c t i v e of p r e s e n t i n v e s t i g a t i o n i s t o p l a c e on r eco rd

tl^ heavy mineral s t u d i e s i n t h r e e l o c a l i t y namely: Shergarh,

i-lahavan, and Agra i n t h e r i v e r sand . The pe rcen tage of

each heavy mineral s p e c i e s i s g iven i n t a b l e 3 . The mine ra l s

as recorded from v a r i o u s l o c a l i t i e s i n o rde r of abundance

a re Epido te , Garnet , Muscovite, Z i r c o n , Kyani te , Tourmaline,

Tremol i t e , A c t i n o l i t e A p a t i t e , Hypers thene , S i l i m a n i t e ,

Hornblende, B i o t i t e , Z o i s i t e , R u t i l e , Anda lus i t e , Opaque

e t c . Their d e s c r i p t i o n i s given below:

DESCRIPTION

Epidote:

Epidote i s the dominating mineral of the heavy mineral

assemblage cons t i tu t ing about 33^ a t shergarh, 25>4 at

Mahavan and 49/c a t Agra, with an average 39i4. The grains

are general ly elongated, pr ismatic and ro\iaded. Two v a r i e t i e s

of epidote/ colour less and coloured are dis t ingoished. The

coloured grains show weak pleochroism, high re f rac t ive index,

and one of yellow and greenish yellow in colour .

Garnet

Garnet i s the next i n order of abundance. I t cons t i tu te

14? a t Shergarh, 26% at Mahavan and TA at Agra, with an

average of about I6;i . Two v a r i e t i e s of garnet are d i s t i n ­

guished namely pink and colot i r less . The pink garnet i s

more common than co lou r l e s s . Majority of grains are

equidimensional, angular to subangular showing considerable

conchoidal f rac tu re .

Mascovlte

The grains are flaky colour less and t ransparent ,

Muscovite forms about 12% of a t shergarh, 11.2J4 a t

Mahavan and 956 a t Agra.

Zircon

Zircon is more frequent at Agra (9%) than Shergarh (6%)

and Mahavan (5%) with an average of about 6.7% , Three

varieties of Zircon are identified^ colourless, pale pink

and palae brown. Zircon occurs as elongate prismatic and

equidimensional g ra ins . Needle l i k e inc lus ions are cornnon.

Kyanite

Kyanite occxirs i n long^ th in , blade l i k e cy l ind r i ca l

p r i smat ic grains with rectangular o u t l i n e . There are two

v a r i e t i e s , colourless and pink. Majority of gra ins are

co lou r l e s s , some gra ins have l i g h t pink or pale blue

colour and are weakly pleochroic showing two se t s of per fec t

c leavage. The content of Kyanite va r i e s from 4,5% a t

Shergarh, 5.3?^ at Mahavan and 7% at Agra.

Tourmaline

Occurrence of tourmaline i s l e s s in Shergarh (3%) and a t

Mahavan (3%). I t percentage decreases in the down stream

side and disappear a t Agra. The grains are green and pale

green in coloxir and are s t rongly pleochroic , pr ismat ic

and sxobrounded to well rounded. S t r a i a t i on are p a r a l l e l to

the pr inc ipa l ax i s . The gra ins become e x t i n c t p a r a l l e l to

the s t r a i a t i o n .

Tremollte/Actinolite

Treraolite occurs as colour less and white and shows

pa le green colour. The grains are sub angular to sxibrounded

with fibrous aggregate and inc l ined ex t inc t i on . The average

content of t remoli te va r i e s from 0,5 to 1^1%. White

a c t i n o l i t e i s found only a t Mahavan and cons t i t u t e 2.65i .

Apa t i t e

I t i s coloxirlesS/ rounded to well rounded, but some

gra ins shows hexagonal form. I t gives f i r s t order grey-

in terference colour and in cross-nicol i t becomes dark due

to very low birefrengence. The average value of a p a t i t e

va r i e s from 0.24 to 0.6X from Shergarh to Agra.

Hypersthene

Hypersthene i s grei ' ish green in colour . The grains are

subangular to subrounded with f rac tures , pleochroic and shows

s t r a i g h t ex t inc t ion . The average value of hypersthene va r i e s

from 0.14% to 0,75?i.

Sl lHtnani te

The grains are co lour less , subangxilar to subrounded with

s t r a i a t i o n s and show s t r a i g h t ex t i nc t i on . The average value

va r i e s from 0.77 to 1,02% from Shergarh to Agra.

Hornblende

The hornblende g ra ins show c h a r a c t e r i s t i c green coloxir

and are pleochroic. The grains are elongated and

irregularly terminated. Some grains show deep colour in

the middle and becoming gradually pale towards boundaries.

The average value of hornblende varies from 0,14 to 0.3%

from shergarh to Mahavan and it is absent at Agra.

Biotite

The b io t i t e grains are bronw in coloxir with perfect

cleavage. I t occurs as flaJces, subrounded, and s t r ia t ions

are coiinionly observed. The average value of b io t i t e i s

1.5/i at Shergarh, 6.8/i at Agra, but i t i s absent at Mahavan.

Zolsite

Zoisite grains ^ p e a r usually prismatic and show two

se ts of cleavage. The polarization colours are inky blue

with inclusions of anphibole microl i te . I t i s present onlv

a t Mahavan (1.26?6) .

Rutile

Rutile occurs as brick red and yellow in colour with

dark boundaries. The grains are subangular to subrounded

in outlines with high rel ief , weak pleochrosira and paral le l

extinction.

Andalasite

I t i s colour less shows weak pleochrosim, p a r a l l e l

ex t inc t ion and are i r r e g u l a r in form. The average value of

andalus i te var ies from 0.35 to 1 , ^ from shergarh to Agra.

Opacpae

Some minerals remain dark in plane polar ised l i g h t .

These are opaque minerals , and no a t t enp t has-been made

to coxint and to iden t i fy them sepa ra t l y .

SOOHCE ROCK CCMPOSITION

The heavy mineral species as recorded from Shergarh,

Mahavan and Agra along the course of r i v e r Yairuna are, by

and l a rge , s imilar in con^josition, inplying tha t a s imi la r

provenance existed for the sands of Yanruna r i v e r in the

study area .

Epidote and garnet which occur abundantly in the study

area, suggest t h e i r der iva t ion from medixim to high grade

s c h i s t s and gneisses rodcs (Krumbein and Pe t t i john , 1936;

Folk, 1961; B l a t t e t a l . 1982 ; Friendman, 1982). Contribution

from basic rocks i s indicated by the presence of epidote,

opaques and r u t i l e . Tourmaline may have been de r ive ! from

gran i te and pegmatit ic rocks (Bla t t e t a l . 1982, Casshyap and

Ahmad, 1987 7 Tewari, 1989}, Although occurring in small

amoxant minerals l i k e b i o t i t e , c h l o r i t e va r i e ty , kyani te and

s i l l i m a n i t e may have t h e i r der ivat ion from low to high rank

metamorphic rocks and some minerals l i k e may

have the i r der ivat ion from mafic igneous rocks (Pet t i john 1975

p 487) .

Thus, the heavy minerals i n the study of r i ve r Yamuna

between shergarh Agra revea ls source rocks of mixed con^osition

comprising l a rge ly of acid p lu tonic igneous rock and raedixini

to high rank metamorphic rocks of sedimentary and igneous

de r iva t ion . These rocks cont r ibute tlie g rea te r and l e s se r

Himalayan ranges which provided the bulk of the sediments to

the Yaimna in the study area.

CHAPTER - VI

WATER AND SEDIMENT POLLUTANTS

GENERAL STATEMENT

In order to assess the water and sediment po l lu t an t s

in pa r t s of r i v e r Yamuna, 'Western U.F./ e igh t sampling

s t a t i ons were es tabl i shed throughout the s t r e t c h of study-

area during the months of April and May 1989. The water

and sedimsnt sanples were co l l ec ted and chemically analysed

in the Geochemical Laboratory of the Geology Department,

A.M.U., Aligarh.

WATER POLLUTANTS

Method o f C o l l e c t i o n

The Water samples for the ana lys is of r ad i ca l s and major

ions were co l lec ted in a well cleaned one l i t r e capacity

double stopped polythene bo t t l e s and subsequently, these .

b o t t l e s were capped and sealed with wax in the f i e l d .

For heavy metal determinations samples were co l l ec ted in

separate t\-K) l i t r e capaci ty polythene b o t t l e s . This group

of v/ater sarrrple was acidif ied with 10 nol 6N HNO a t the s i t e

immediately and then capped and sealed with wax as above.

Analytical Procedure

The samples were analysed as per standard method

recorrmended by APHA (1975) . For heavy metal ana lys is , 500 ml

f i l t e r e d sairiples were acidi f ied again with 5 ml of 6N HNO

and concentrated up to 50 ml a t low temperature (Parker, 197 2)

The r ad i ca l s l i k e carbonate, b icarbonate , chlor ide , and

t o t a l hardness as CaC03 were determined using volumetric

methods. Sulphate was determined by gravimetric method. The

major elements l ike sodium, potassium, magnesivim, calcium

and t r ace elements l i k e Cr, Co, Cu, Cd, Fe, Ni, Pb and Zn

were analysed using GBC -902, Double Beam Atomic

Absorption Spectrophotometer. A blank sample was made for

each spectrophotometric analysis i n order to account any

ana ly t ica l and instrumental e r r o r .

Result and Discussion

The concentration of d i f ferent m^'or elements and

r a d i c a l s of water sanples a t var ious sanpling s t r a t i o n s

(Fig . 2) i s presented in Table 4 and those of t race elements

are given in Table - 5. i^e Table 6 shows the comparative

ti a.

0) t-H J 3 ID

6-1

to u

in in (11 L:

r I '

I) 0)

•D U u HI K

tn 03

« +J c 0)

a d) rH a) i-( o ••- ra B

•u c ID

10 .H ra (J

1 (^ o o D'

1 1 n t ) U

\ C 0 •H X.

a B '.' u 10 E

a; l i .

u. a ra

o o • J

c o

• H 4J

ra

CO o en

o o

o ON m CM

o

IT) ON

CO

o

o

o

o

0

CD

O 01

03 in

in

o ID

<31

OO rH r^ 00 00

CO 00

O

CO

o

o o

t-^ \D r~1

IJ) lO

l O CO

o 00 CO

h ro (11 t j +j VI u, D

10 01 u JJ to c ,« (1 u

h ID (1) M +J CO t i . :3

ra (U M -p 10 c : 0 i-i

h ra «) u P 10 u :o

4J ra ^ o

K

^ O (K W 3-: in

cc D

r -:: f< J :3 in

D a;

•:S o

N O

X o M

10

U1 O

CO

o o

M r: ra i j

c M 11) •P in nj i j

e <0

{J in c o Q

M u ra w

K 1-1 ID JJ n 111

"

M l^ ra

XI

c u ID

4-> in ra 10

h ro ai u in

D

+J M o u. u (0

" • '

^ ra x: ro >: ••-)

ra H

13 c:

• H

ai ra

>: u (0 JJ

c M 01

« Ul ra

10 j c : ra en

ID

a 'O

a) en

X u m X)

c V4 gi 4J (0 01 •t

j r ; t : ra n

r; u Q) p in ra w

0)

•H

Jd U ra JJ

n M OJ •p m 01

.

X c in fl

c u 01 •p in m

I d

A: c m ^ c M OJ P 10 01

s

-H L I

CO

to

oi w

M

rH

• D «> 9) C > 3 M B (i) m w >-<

ja O U-(

o a o u •H tt) 4-> -P (0 to H >

• P C (U 0) £ O 4^ C O C U -H

;C B •P O

<a -p (U n>

X (0 •w

-o c r-i fO u en o u » o

(0

•o Id c T ) O

m-p -P 3 w+>

i H C + J n) n

•r< C - O H

c H

r

• u 0) >

t ^

u - 1

^ « <!> e -H > 3 OT Q)

^ • g " X M 0) (0 0) -H

s a,Q . ^ tt) ^

^ 00 *i Xi a\ to nj .-1 0) M - ^

x : -H »H CP « <U

•H (U > a: -a (u

rH V

<H 43 •H

E (0 3 to e r i "H

•H b tt) X M > (0 0) 0)

S a n ^ • * »

m 0) 00

rH 0» +» 43 rH (0 n) - ' «) Ul rH

x : - H 0) en w >

•H • « tt) K -O H

CO p c (U 3

4J • H 4J m c o U

U

2! •

o No

CO

--: w

cr I IP si)

o

CD VO

VO

CM in

o o m o VO n

in

in

o VO VO

l- rH

ID

in

o VO ON

m

o

VO

in

CM in CM

iS r

o o in

o o

o in rH

in

o n

rH

O

in o o

o o

o CN

o

rH m o o o o o o

o o VO

in O rH • •

o in o o o o t I o rH OJ

in o • •

O O O rH rH O O O O O VO (N rH O

O o

o o

m rH tt) U C o

O -H

1(1

00

1 U)

o o ro

O r-

O n

i n

o • o

• o o

i n o i n

in o

8 10

u n (0

B a o. 10 m tt) B

XJ U (d K rH ro

+J X O a fH

1 a ^

E 3

• H U

r H

ro u

1 a a

^ - i "

E 3

• H to 0) B

cn ro 2

-g a a

u 0)

a a o u

-g a a

B O

u H

-g a 3 tt)

-D • H M O

r H

£ O

E a 04

tt) -p to

4=

a r H 3 to

-g a a

E 3

•H E

X)

ro u

-g a a s ^

-o ro tt) ^

-g a a "E 3

•H E O

u

+> B tt)

H

ro > ro X tt) X

and 90 ppra a t Mathura, Shikohabad s t a t i o n s .

4 . Bicarbonate:

The bicarbonate concentrat ion was foxind i n the range

of 237.60 - 474.50 ppm with the highest value of 474.5 ppra

a t Agra (near Taj Mahal) .

5 , Chloride:

The chloride concentrat ion was reported in the range

of 239.60 - 475.95 ppm. The highest value was recorded at

Agra (near Fort) . I t has been observed tha t the chlor ide

concentrat ion i s higher than t h a t of highest des i r ab le

l i m i t described by ISI (1983) .

Indian Council of Medical Research (1975) while

recommending 200 ppm a des i r ab le l i m i t of ch lor ide in potable

waters has also l a i d down 1000 ppra as the maximum permissible

l i m i t where no other a l t e rna t ive soxirce i s a v a i l a b l e . High

concentrat ion of chlor ide gives an undesirable t a s t e to water

and beverages. On account of t h i s high concentrat ion of

ch lo r ide , infants and young chi ldren may get t h e i r de l i c a t e

kidney t i s sues damaged by the higher osmotic p ressure brought

about by the presence of high concentrat ion of s a l t s . So,

i t i s necessary to keep the chlor ide content as low as possible

in water suppl ies .

6 . sulphate:

The concentration of sulphate ranges from 252.75 to 547.70

ppm. The higher values of sxiLphate were observed i n Shergarh,

Sxiltanpur and Mathura v*iich may be on account of sodixiin

sxilphate. Mahavan> , Agra, Firozabad, Shikohabad and Etawah

sampling s ta t ions are showing lower va lues , which may be due

to l e s s oxidation of sulphide to su lpha te . Almost a l l the

samples show the higher values than permiss ible l i m i t of

250 ppm. (Table 4 ) .

7 . Total Hardness as CaCO^:

The to t a l hardness ranges from 170 ppm to 402 ppm. All

the water sarrples have shown t h e i r values well within the

l i m i t s described by 131 (1983) and VftiO (1984).

8 . Sodium:

The concentration of sodium depends on various fac tors

such as i ndus t r i a l a c t i v i t y , hydrogeological condit ions and

season of the year in the area, sodium i s a lso responsible

for increased incidence of high blood p r e s s u r e .

The concentration of sodiiim in the study area i s found

7:

ranging between 225.70 to 403.10 ppm. The highest

concentrat ion was recorded a t Agra behind Taj Mahal, The

values around 200 ppm may be harmful to person, suffering

from renal / cardiac and d iseases r e l a t i n g to c i r cu l a to ry

system. The higher values of sodium were obtained in a l l

the water sanples .

9 . Potassium:

Mo desi rable or excessive l i m i t for potassium has been

s e t so fa r . The potassium concentrat ion ' ranges between

25.00 to 80.20 ppm. The highest concentrat ion (80.20 ppm) was

recorded atAgra (near F o r t ) .

10. Calcium:

The concentration of calcium ranges between 16.68 ppm to

46.36 ppm. The highest concentration of calcium was recorded

(46.36 ppm) at Mahavan (eastern bank) .

The calcium plays a v i t a l ro le in the growth of human

body which requi res 0.7 to 2.0 gram per day. Lactat ing women

and growing children may require l a rge r doses . The hard water

with high calcium concentration may cause ur inary d i so rde r ,

whereas very soft water without calcium i s responsible for

r ecke t s , tee th decay e t c . The water having 100 ppm of calcium

i s not considered harmless. The values of calcium in the

study area are found vd.thin the permissible l i m i t .

1 1 . Hagnesitim:

The concentration o i magnesixira .ranges "115.45-- 350.30 ppn

The highest value was foxind a t Agra near For t . The values

of magnesium are higher than the permissible l i m i t (ISI, 1983).

However, the high concentrat ion of magnesium has laxa t ive

e f f e c t .

Trace Slements

The t r ace elements are those elements which are found

in very low concentra t ion, i n s p i t e of t h e i r low concentrat ion,

they play a /:ey ro le in the d i e t s of hximan and animals and

for the healthy growth of p l a n t s . 3ut a t higher concentrat ion,

these elements may become in jur ious or even toxic to the

organic l i f e . The r e s u l t s of tiiese t race elements are

presented and discussed as follows:

Chromium:

The concentration of hexavalent chromixim was found in

the range of .0003 - .0270ppm. The h ighes t concentration of

chromium was observed near Taj Mahal a t Agra. The water

sanples of a l l the sanpling s t a t i o n s show chromixira concentration

within the des i rab le l i m i t of ISI (1983) drinking v/ater

s tandard.

Copper:

The copper concentrat ion was detected in the range

ND-0.0152 ppm. The h ighes t ccxicentration was found behind

Taj Mahal/ Agra. The water san^iles show the copper concentration

within the des i rable l i m i t of ISI (19 83) and WHO (1984)

dr inking water s tandards . The high copper concentration in

Agra and Mathura area can be a t t r i b u t e d to la rge scale

nonferrous mstal i n d u s t r i e s using copper a l l o y s .

Cobalt :

The concentration of cobal t ranges between O.OOOl ppm

to 0.0006 ppm. The maximum cobal t concentrat ion was found at

Firozabad. Cobalt does not play much iii5)ortant ro le in human

metabolism.

Cadmium:

The cadmium concentrat ion ranges between 0,0419 to 0.3330

ppm. The maxLmam concentrat ion of cadmiiim was determined a t

Mathura (Western bank) . The nonferrous i n d u s t r i e s use cadmium

corrpounds in the various i n d u s t r i a l process may account for

high concentration of cadmium.

Much at tent ion sho\ild be given to the cadmium because i t

i s highly toxic and widely d i s t r i b u t e d in t races in the envi ­

ronment. The high concentrat ion of cadmium i s a deadly poison

but a small amoxint of cadmium taken over a long period of

time accumulates in the body and causes ser ious i l l n e s s

CVerma, M.M. 1987) .

I r o n :

The concentration of i ron ranges from 0.1660 to 0.7140

ppm. The highest concentrat ion was found a t Mahavan (eas te rn bank

All the sanples snow i ron concentrat ion above the de s i r ab l e

l i m i t of WHO (1984). However, except few almost a l l the

sanples have higher values than the des i rab le l i m i t s ( I , SI 1983).

The high concentration of i ron may De on account o f (e f f luen t s

discharging (the i ndus t r i a l and domestic) i n to the r i v e r . Iron

i s very inpor tan t element in human n u t r i t i o n but becomes very

tox ic when administered p a r e n t e r a l l y (Fairbank e t a l . , 1971).

Z inc :

The Zinc concentration ranges between 0.0200 ppm to

0.7490 ppm. The highest concentrat ion was-:reBQ**^ a t A^ra

near Fort* Industrial v;aste water may be the possible source

of zinc in the Yamuna river water.

Lead;

The lead concentrat ion was found in the range of 0.0001

to 0.0011 ppm. The h ighes t concentrat ion was determined near

Fort a t Agra. The lead concentrat ion was found l e s s than

l i m i t s of ISI (1983) and WHO (1984) s t anda rds .

Lead i s one of the hazardous and p o t e n t i a l l y harmful

po l l u t an t s with i t s impact on organism. Lead poisoning

symptoms usual ly develop slov/ly with i n t e s t i n a l cranps,

per iphera l nerve pa ra ly s i s , anaemia. I t causes mental

r e t a rda t ion among chi ldren, increases abortion r a t e s and

i n f e r t i l i t y in males.

SEDIMENT POLLUTANTS

Method of Col l ec t ion

Soil and sand sarnies were co l lec ted in 100 grams

capaci ty polythene pacJt a f t e r digging down to depth of one

meter upper surface of sand and so i l along the r i ve r course

from the 13 sampling s t a t i o n s se t uped in the en t i r e b e l t of

the study area .

Apalytical procedore

The sediment sarriples were a i r dr ied for 24 hours, ground

and passed through an 80 mesh s i eve . Five gram of the sample

was reflued with 20 ml. cone. HNO for two hours . The san5>le

was cooled and brought to 50 ml. volume with 2% HNO and

f i l t e r e d solution was analysed by GBC-902 Double Beam Atomic

Absorption Spectrophotometer (Parkev:, 1972) .

Resu l t and Discussion

The concentration of major elements and t race elements

are given in the Table 7 and 8 r e spec t ive ly . Table 9 reveals

the comparative study of ce r t a in po l lu t an t s with mean world 's

sea sediment concentrat ion.

Mad o r Slemesnts

Various major elements from the sediments of Yamuna r i v e r

were determined are sodium, potassium, calcium and magnesium.

Their r e s u l t s are presented and discussed below:

The concentration of sodium, potassium, magnesium and

calcium in the sand ware found ranging 75,35 - 335.85, 19,95 -

78.65, 165.23 - 602.00 and 10.48 - 176.00 ppm r e s p e c t i v e l y . The

maximum concentration of sodium was detected a t Firozabad;

Sultanpur (upstream) has shown the maximum concentra t ion of

E a o. Oi,

H

a: < 2

§ < >^ fx4

o w e g H Q W CO

H K B Z H W

g H I-] W Cki o •^ 1 ^

^ ( o z o H H < «

o z 8 ••

c~ 0) rH

•s B

1 -H

n) U

£

i4

(0 2:

•H O tf)

-o C n) OT

•H •H O W

TJ C

to

r-^

•H

o (0

-a c (0 to

•H -H

o to

X) B IT) to

c o •H +J ro +J V)

CP c •H rH

@« e ro

VO n

in rf

TH VO

(X) ro

ro OJ

r» 00 ro

ro in

in 00 ro

Oi 00

O • *

CO CM

VO ro

in ro

«-H O ro

O in

OJ

o ro

1 <tJ (U u +J m D, 3

• " . ^

x: M n) t? M (U JC

<M ro

»H VO

VO in

a\ ro

in

o 04 rg -*

O t n eg • ^

O t~-

VO in

in VO

«-» •«t

o T»<

o rH ro

O

r CM CM ro

E (0 0) l-« +J n c S o TJ ^^

x: M 10 O" iH (U £

VO ro

CO CD

CM t

t •'f

in in

CM O •«1'

in • < *

r-i

00 ro

in o in M-

in VO

CO r-

o en <j\ TH

ro

in

r in ri

ro

'B (0 <U U +> to o« 9 •"^

u 3 a c (0 4J <-( a

o o r "<i<

CM in

in c

o in

TH

VO in

o ro t--CJ> -«*

o CM in ro

in ^

cy> CM

in CM

rH 00

o t

ro ro CM

(0 0) M -P to c 5 o TJ ^^ tH 3 Q. C to -p rH 3

O • ^

in rM

^ CM

ro CM »H

o CO

TM

o f>J

o t'-in

c ro

ro in

c CM

00 ro

in <M

0\ ro

c VO

in ro

in r

^—>

e (0 (U In •p (0

a 3 • — »

<0 Ul 3 x: 4J (0

o 00

ro ro

VO CTv

• *

in y-i

in 00

<^ o Tf

o o CM

o VO

o CM «-H

m

o VO CM ro

in rf

00

r

in o\ TH

CT\

i-^fc

e (0 (U l4 -p n c 3 O •o v.^

(0 M 3 x: +J in

o CM

r-ro

CM ro

C^ ro rH

o r r-00 CM

o in 00

o in

in CM

VO

c

o r-VO • ^

in CTi

"I*

a\ CM

O

o o ro CI

C ro > (0 £ m

1

^ 00

in cr>

1

in CO

<j\

in •*

1

in CM

•«t • *

1

o r CO

r CM

x-> B <d (U u •P (0

a 3 >_»•

(0 M t-n

VO in

1 • VO

o rH

o r>j o r-

VO CO r~ CO rH

o in •

1 VO 0\ in

^ o VO CM

r- •* (T\ t^ rH ^

in CO

1 • rj r-

o in o o VO CTi •<* ro

o CO •

1 • ^

in CM

in o CM o

VO ro r- in CM CM

X-**

^ e 4J 10 U 0)

o u PM -P

n }3 § 0) O c -o v-» ^-»

(0 <0

u u rx\ f-tv

^ •

in CM

CO CM

CM T-l

O in • CM ro ro

O o

c •<*• •*

o 00 •

00 rH

O in

r«4 ro

o o • o VO ro

in 00

in ro CM

OJ (0 JQ (0 N O M

VO CM •

in »-H

CO rt

O rH

CM VO • "* CN CM

O in CM

n CM

r-r~ •

rH CM

VO Ti­

ro CM

ro in •

in 00 CM

CM vO

ro c CM

X) to X> (0

s: o M •H f

CM

r • t-t

CM

o •t

r~-CN

in CM • ro • *

rH

in CM

in VO r-i

in o •

00 1-i

m <^

a> rH

o o\ • in CM CM

CM

r vO m CM

x: (0 » (0 1 1

o 03

CO •X) i n o

in CO in

o

00

o r-o

r-m CM O

C 10

o r- o

£1 0.

o (0

c

10

ir> ID O

1

o

<N

o •

O

M O

• o • *

IN O

CM O

•

CM O

o to

B 10 10

o CO

o o

o o

o o o

o

rj* (N o o o o

CN O

''

u a CM tf CM O

•

CM O

• c o o o »

D ts

CM O

• CO

o o o •

CM

•* o o •

CN

o •

(J> ro O O

• «H CN rH

n •

c 10 (0

o o o o

o o

o o o

o o o

01

o (O

O CD O 1 0

CO

o

o o

o 00 o

o GO CO

s o to

c

to

o

c m to

o o

o

»H CO CO 0\ o o

o o o

o o o

o

CO i n i n

en o

r-o

ID O

ID O

O O

o o

o o

o o o

o o o

00 o o o

CJ>

o o

i n o o

CM

r-in o

1

r-CD

a\ o

. ID O

o o

o o o Q

00 • *

0 \ lO

i n o

lO

o C3 O

• fH rH O O

r~ o o o • o TH

o o

CM O O O

• 10 •0'

o o

(0 u c a) u c: o o

3 U

O

o to

C 10 to

o to

c 10 to

2

o o

o o

lO 0)

o o

c-(r\ o o

o

Q 2!

:3

O o

o o

to o o

o o

o o o

in

o o •

1

ID O O

• * ^ .H O

a •z

tT> CM t~-O

U s CO 0^ O O

CM

o o •

CN lO tH O

VO vo I - rt •-1 CO

10 (U

0 \ P -CM r - l

Table 9 : Comparison of certain Trace Elements with Mean

Worlds' sea sediment values ppm •

S . M O . T r a c e e l e m e n t

Mean W o r l d ' s s e e s e d i m e n t c o n c e n t r a t i o n

Min . Max

Study Area sand

Min Max

S o i l

" i n Max.

1 .

2 .

3 .

4 .

Cd

Cu

Pb

Zn

0.0

0^002

0.0003 .0253 .1650 .0322 .1280

0.1920 ND

1.0

.149 ND .0019

0.0200 .0216 .1564 .0149 .0403

.0185 .1100 .0209 .1102

0.1280, 0.0149 - 0.0403 and 0.0201 - 0.1102 ppm respec t ive ly .

The raaximam concentrat ions of Cu, Co and Cd were foiond a t

Etawah/ Hathura (dovmstream) and Sultanpur (upstream)

whereas the maximum concentrat ion of Pb and Zn were repor ted

a t Mahavan.

The Rankaraa and Saharaa (I960) have repor ted the mean

concentration of the ^.•forld's sea sediments for the t race

elements l ike Cd, Cu, Pb and Zn are 0.0003, 0-0.19 20,

0.0200 and 0.002 - 1.0 ppm re spec t ive ly (Table 9 ) . The

sediment sariples of the study area were con^ared with mean

World's sea sediments concent ra t ion . The concentra t ions of

Cd and 2n were foiind lower than the mean World's sea

sediment concentration whereas concentrat ion of Cu and Pb

were higher than mean ' .Grid's sea sediment concentra t ions

except so i l of Sultanpur downstream.

Chromixim, Iron, Manganese and Nickel;

The concentrations of Cr, ?e, Mg and Ni in the sands

were found ranging 0.0057 - 0.0363, 0,0591 - 0.1433,

0.0039 - 0.0394 and ND-0.4400 ppm re spec t i ve ly with t h e i r

maximum concentrations a t Mahavan, Agra, Mathura and

Shergarh respec t ive ly .

In case of s o i l t h e c o n c e n t r a t i o n of Cr, Fe, I-ln and

Ni were foxmd ranging 0.0027 - 0 .0729, 0.0292 - 0 .4400,

ND-0.440 and ND-0.0052 ppm r e s p e c t i v e l y . The maxiinara

c o n c e n t r a t i o n of Fe and Mn was d e t e c t e d a t s h e r g a r h

(upstream) ^ e r e a s uiaxiimim Cr and Ni were found the h i g h e s t

a t F i rozabad and Mathura r e s p e c t i v e l y .

8i

aamU&Y ASD CC»ICLUSIONS

The main conclusions of t h i s inves t iga t ion as here

obtained should be t r ea ted as t en t a t i ve , subject to a

fu l l e r study over a bigger a rea . These conclusions are

sununarised below:

1. The study r e l a t e s to the Yamuna r iver , a t r i b u t a r y of

the Ganga River, over a s t r e t c h of about 125 km a t

Shergarh, Mahavan (Gokul), Agra and Etawah in the

western par t of Ut ta r Pradesh, the study was undertaken

with special reference to bed forms, t h e i r fac ies ,

tex ture , bedding type, and coiiposition, in r e l a t i o n to

mode of t ranspor t and deposi t ion by a meandering of

a high s inuos i ty .

2» The Yamuna r ive r exh ib i t s meandering pa t t e rn between

Shergarh and Stawah, and shows various geomorphic

fea tures , l i k e point bar, marginal bars v e r t i c a l

accretionary deposi ts , A Veneer of wind blown sand

showing t r a ins of symmetrical r i p p l a s are well developed

along the r ive r banks.

The deposit ion of poin t bars and marginal bars c l ea r ly

shows tha t they are formed when the r i v e r channel migrates

l a t e r a l l y / vrtiereas the t r a i n s of accret ionary bars (width

about 50-70 m) developed along r i v e r Yanuna/ follow the

t rack of the meander channel . A close examination shows

t h a t these f luvia l deposi ts cons i s t mostly of sand and

occupy the marginal boundaries of an act ive channel. The

upper p a r t of these bars i s f l a t flood p la in surface which

cons i s t s of fine sand and s i l t . The v e r t i c a l accret ionary

depos i t s are formed as a r e s u l t of s e t t l i n g of suspended

load from flood waters. The overbank v e r t i c a l accretionary

deposi ts cons i s t of fine grained sediments and are well

developed in the proximal levees along s teeper concave bank

and in the d i s t a l back swamps.

3 , Ver t ica l as well a s l a t e r a l associa t ion of sedimentary

fac ies in point/channel bars e ^ o s e d due to sh i f t ing

of r i v e r course and f a l l in water l eve l shows tha t they

abound in super in^josed dunes, bars , r i p p l e d r i f t ,

asymnetrical luna te and l ingouid r i p p l e s .

4 . Eight facies were recognised on the basis of f i e l d s tudies

of r i v e r Yamuna and coded ind iv idua l ly following the

modified scheme of Miall (1978) . They a r e : (1) Planar cross

bedded facies (Sp) (2) Trough cross-bedded fac ies (St)

(3) Massive to hor izonta l laminated fac ies (sro-sh);

(4) Channel f i l l f ac ies (Sch) (5) Ripple - laminated to

r i pp l e d r i f t laminated fac ies (Sr) (6) Convolute

l&minated facies (Fc) (7)'. Massive <mM.ci -^©.ciei ( ^ ^ w )

(8) P a r a l l e l laminated f a c i e s (sl) .

Indeed/ the deposit ion in t he channels has been taking

place in the d i s t i n c t i v e phases . The coarser f ac ies

such as planar and trough cross-bedded sands and hor izonta l

laminated sands .seem to have been deposited in the flood facies

s t age . The Planar and trough cross-bedded/are governed by

deposit ion during migration of t ransverse bars and dunes

respect ive ly , whereas the hor izon ta l laminated sand was

deposi ted in the plane-bed phase of the upper flow regime.

The f iner facies such as r i p p l e laminated to r i p p l e d r i f t

laminated sand. S i l t and mud, deposited during the

f a l l i n g stage, may have reworked tops of bars to from

cross-laminated sand fac ies as observed in channels a t

the p resen t . Convolute laminat ion may have formed in

d i f f e r en t ways. In the study area, these laminations

are formed by the escape of the water a f te r deposi t ion

of the sediments or by d i f f e r e n t i a l load . The general

due to the fact tha t the source area may have undergone pro­

longed erosion and sediment so derived on reworking have

become b e t t e r sorted._

6 . Heavy mineral assemblage does not show any s i g n i f i c a n t

va r i a t i on in species from shergarh to Agra, i t i s perhaps

because of smaller a rea . Seven t een^ - heavy mineral

species including opaques have been i d e n t i f i e d of vrtiich

more abundant are epidote, garnet and kyanite and l e s s

abundant are Muscovite, Zircon, Tourmaline, Tremolite,

Act ino l i t e / Apatite, Hypersthene, S i l l iman i t e , Hornblende,

B i o t i t e , Zo i s i t e , Rut i le , Andalusite, opaque e tc given

i n table 3 .

7 . Heavy mineral species suggest t h a t the sediments were

derived la rge ly from older g r a n i t i c gneisses and s c h i s t

of medium to high grade metamorphic rocks occuring

approximately ^'^S'oo Km in the northen p a r t of the

study area.

8. As far as water po l l u t an t s are concerned pH values are

within the l imi t s (Tabic ^ ) • The values of pH revea l

the a lkal ine nat:ure of Yamuna r i v e r water . The values

of e l e c t r i c a l ccnduct ivi ty ind ica te t h a t the water of

Yamuna r ive r i s moderately mineral ized. Almost a l l the

ca t ions and anions concentration are well ^d.thin the

permissible l i m i t s except sodium and in some cases

magnesiiim and Sulphate which show higher values as

recorded at places in Yamuna water, and may be in ju r ious

to animals and p l a n t s .

The trace element concentrat ions are found i n t he i r

permissible l i m i t s except values of Ca and Fe. In case

of sediment the high values of Na and K were obtained

vrtiereas in case of t race elements the Fe, Cd and Mn

show high concentra t ions . The r e s u l t s show t h a t there

i s a considerable var ia t ion of water and sediment

po l lu t an t s from one san:5)ling s t a t ion to other which may

be on account of var ia t ion in the quant i ty of i n d u s t r i a l

and dov<n s i t e wasres being added to the Yamuna r i v e r a t

d i f fe ren t c i ty c en t e r s , Indian r i v e r s carry huge

i n d u s t r i a l and metropolies wastes round the year.

REFERENCES :

A a r l o , R. 1971 - 3 u l l . Gecl Soc . F i n l l . V. 43, p . 163-172.

A l l e n , J ' .R.L. , 1962 - A symet lca l r i p p l e marks and t h e o r i g i n

of c r o s s s t r a t i f i c a t i o n s , .

N a t u r e . V. 194, p . 197-169 .

A l l e n , J . R . L . , 1963 - The c l a s s i f i c a t i o n of s t r a t i f i e d xanits,

with no te s on t h e i r o r i g i n of c r o s s s t r a t i f i c a t ­

i o n s , Natxire. V. 194, p . 93-114.

A l l e n , J . R . L . , 1965 - A review of t h e o r i g i n ind c h a r a c t e r i s t i c s

of r e c e n t a l l u v i a l sed iments , Sedimentology,

V. 5, p . 8 1 - 9 1 .

A .P .H .A . , 1975 - S tandard method for examinat ion of water

and waste w a t e r . 14 Edu. Am. P u b l . H e a l t h . Assoc .

Washington, D.C,

B l a t t , H. 1982 - Sedimentary P e t r o l o g y . Freertan and Conpany,

san F ranc i sco , New York, p . 568.

B r i d g e , J . S . , 1978 - Origin of h o r i z o n t a l l amina t ion under

t i a rbulen t boundary l a y e r s . Sedim. Geol . V. 20,

p . 1-16.

B r i d g e , J . S . , 1985 - Paleochannel p a t t e r n i n f e r r e d from a l l u v i a l

d e p o s i t s : a c r i t i c a l e v a l u a t i o n . J o u r . Sedim.

P e t r o l . V, 55, p . 579-589.

Bucher, W.H., 1919 - On r ipp le s and r e l a t e d sedimentary surface

forms aiid t he i r paleo-geographlc I n t e r p r e t a t i o n .

Am. J o u r . Sc i . V. 47, p . 149-210 and p . 241-269.

Casshyap, S.M, and Ahmad, I . , 1987 - Heavy mineral d i s t r i b u t i o n

of lower Gondwana rocks of J h a r i a C.F. Bihar

Ind. Mlneralo. V. 27, p . 95-111 .

Collenson, J . P . and *rhonpson, D.B., 1982. Sedimentary structxires

p . 97.

Doeglas, D.J. 1946 - In te rp re ta t ion of the r e s u l t s of mechanical

a n a l y s i s . Jour . Sed. Petrology. V. 16, p . 19-40.

Dickinson, WJl., 1974 - P la te t ec ton ics and Sedimentation In :

Dickinson, W.R. (Ed) : t ec ton ic s and sedimentat ion.

Soc. Econ. Paleon. Mineral. Spec. Pup. V, 22,

p . 1-27.

Fairbanks, v . F . , Fehey, J . L . and Bul t le r , E. , 1971 - C l in i ca l

Disorders of Iron Metabolism, 2nd ed . Grune and

S t r a t ton , New York, pp . 486

Fol^K- R.L» and VPrd, W.J., 1975 - Brazos r i v e r bar : A study

in the s ignif icance of grain s i z e parameters .

JSP, V. 27, p . 2-26.

F r a z i e r , D.E., Osanlc A., 1961 - point bar d e p o s i t s . Old River

FolK, R.L., 1961 - Petxology of sedimentary Rocks Herrphills

Austin, Taxas, pp . (154).

Friedman, G.M. 1961 - Dis t r ibut ion between dune, beach and

r i v e r sands form the i r t ex tu ra l c h a r a c t e r i s t i c s .

Jour Sed i . , Pdtroiogy, v . 31, p . 514-529.

Friedman, G.M., 1967 - Dynamic processes and s t a t i c a l pararreters

compared for s ize frequency d i s t r i b u t i o n of

beach and r ive r sand. Jour . Sed. Petrology, V. 37:

p . 327-354.

Friedman, G.M. and Johnson, G., 1982 - Exercises in sedimentology

John Wiley & Sons Inc . p . 62-75.

Fr iend, P.F. , 1983 - Towards the f i e ld c l a s s i f i c a t i o n of a l l u v i a l

a rchi toxture or sequence. I n . J . D . Collinson and

J . Lewin (Edi lors) , Modern and Ancient F luvia l

Systems. I n t . , Asso. sediment, spec. Publ . , v . 6

p . 345-354.

F ie ld ing , C.R., 1986 - Fluvial channel of the Durham coal f i e ld ,

NE England Sedimentology. V. 33, p . 119-140.

Harmxj^'O''Structures and sequences in c l a s t i c rocks_. Soc. Econ.

Pa len to . Mineral. Short course No. 9, p . 3-22.

^ _ ,. 1965 - S t ra t i f i ca t ion , b ^ d

n<ii- '"»'y-- ^,„^na ( w i t h an ej^aiL^xv, -*. ci>m forms, and flow phenomina .witn . . e Rio crade) . Prinery sedia^ntary s t ^ c . u . . .

and the i r .ydrodyna^nic i n t e r p r e t a t i o n . In . a ,> , .

r.d^ soc . Econ. pa lento . y d t e r ^ l . Middleton (ed) . i=oc.

spec. Publ . « o . 12, p . B4-U5.

, , , , . , - S o . . i n , o . s e a . ^ n « in ^ e U ^ . o^ . X . . e

' " ' ^ ^ ^ = . . n i c s . aour . Sea i . P e ^ o . o ^ . V. : , . p . S . - , o .

^ . n ^ r d s , Table-1 subs t ances or . T 1983 - Drinking water standards,

I . S . I . , 1983 effecting the a c c e p t a b i l i t y of c h a r a c t e r i s t i c s effecting

, a t e r for domesUc use, 1983.

^ . , , , , , 5 - Hierachial a t t r i b u t e s and u n i f y i n g

" " ^ ° " . I d e l Of bed forms co^osed of C h e s s i o n l e r s

material and produced . y shearing flow. BuU.CeoI .

XT fl6 p . 1523-1533. Soc. Am. V. 8b, P-

, V 1963 . Hydrolic s tudies on the or igin of beeldlng j o p l i n g , A . v . y p . 115-121.

Sedimentology, v . ^, P»

^<r.n and rasper Formation of the c u 1929 - The Formation and P

K n i g h t , S .H. , ^ ^ ^ ^ ^^ ^ ^ ^ , , 3 3 ^ 3 , ,

haramine Basin . ^ i „ . rn-i publ. Sci. Geol., V. 1,

sediments. Wyo. bni. Pui:> •

p. 82,

Krumbeln, W.C. and P e t t i John, F . J . , 19 38 - Manual of sed lmsnta ry

- - 17^ • f ^ — ^ - w . i w C i .-UCUL y, i-^tw l O r K , p . b 4 y

Kuenen, Ph. H., 1953 - S i g n i f i c a n t featxires of graded bedd ing .

B u l l . Am. Assoc . P e t r o l . G e o l o g i s t s , V. 37,

p . 1044-1066.

Kumar, S .P . and Singh, 1 . 3 . , 1978 - Sed imento log ica l s tudy of

Gomti r i v e r sediments, . U t t a r Pradesh, I nd i a ,

Exanple of a r i v e r i n a l l u v i a l p l a i n Senckenbergian

mar i t , V. 410, p . 145-211 .

Lahee , E.H., 1952 - F i e l d Geology, 5th ed . Mc. Gromel H i l l Book

Co., New York, p . 88 3 .

Mason, C.C. and Folk, R .L . , 1958 - D i f f e r e n t i a t i o n of beach dune

and a e o l i a n f l a t environments by s i z e a n a l y s i s .

Mustang I s l a n d , Taxas, J o u r . Sad. Pe t ro logy ,

V. 28, p . 211-226.

Mcke«, S.D., Enosby, E . J . , B e r r y h i l l , H.L., 1967 - Flood d e p o s i t s ,

Bijon Creek, Colordao . June , 1965, J o u r . Sediment,

Pe t ro logy , V. 37, p . 829-851 .

Mckee, E.D., 1957 - Primary s t r u c t u r e s in some r e c e n t s e d i m e n t s .

B u l l . Am, Assoc . P e t r o l . G e o l o g i s t s , V. 4 1 ,

p . 1704-1743.

p a r k e r , C.R., 1972 - water Ana lys i s by Atomic Absorpt ion

spec t roscopy var ian t e c h t r o n p t y . L t d . A u s t r a l i a .

P e t t l j o h n , F . J . and S i v e r , R. 1972 - Sand and sand s tone , p . 618

Ber l lng Heide lberg - New York : S p r i n g e r .

Quidwai, H.A. and Casshyap, S.M. - 1978 - Grain s i z e c h a r a c t e r ­

i s t i c of a n c i e n t f l u v i a l d e p o s i t s an exanple from

lower Gondwana (Permian) Formation Pench v a l l e y

Coal F i e l d , Cen t r a l I n d i a . J o u r . Geol . Soc. India

V. 19, p . 240-250.

Rankama, H and Sahama, T.G., I960 - Geochemistry, p . 591 . I n t e r -

s c i e n c e , New York.

Re ineek , H.E., 1963 - Der K a s t e n g r e f e r . Natixre Mus. V. 8 3,

p . 102-108 .

Re ineek , H.E. and Singh, 1 . 3 . , 1980 - Depos i t i ona l Sedimentary

environment . 2nd e d i t i o n (Revised) p . 87 t o 130,

Be r l i n Heidelbeg, New York.

R u s t , B.R., 1972 - S t r u c t u r e and p r o c e s s i n a b r a i d e d r i v e r .

Sedimentology, V. 18, p . 221-246.

R u s t , B.R., 1978 - Depos i t i ona l model for b r a i d e d a l l u v i u m . F l u v i a l

Sedimentology, I n . A.D. Miall (ed) Canadian Soc .

p e t r o l l e u m . G e o l o g i s t s . Mem. S . , p . 605-625 .

Mckee, E.D. , 1965 - Experiments on r i p p l e l a m i n a t i o n . In pr i r rary

sedimentary s t r u c t u r e s ana cuexi. H^IIL wJj.i.ia/iviv_

i n t e r p r e t a t i o n , G.V. Mi d i l a t i o n (ed) , p . 66,

Spec i a l P u b l i . 12, S o c i e t y of Economic P a l e n t o -

g i s t s and M i n e r a l o g i s t s , Tulsa , Oklahoma.

Mckee, E.D. , 1975 - Geometry and growth of the whi te sand Dune

F i e l d , New Mexico. J o u r l . R e s . US. Geol . Su rv .

V. 3, p . 51-66.

M i a l l , A.D. - 1978 - L i t h o f a c i e s types and v e r t i c a l p r o f i l e

models in b ra ided r i v e r d e p o s i t s : a summary.

F l u v i a l sedimentology. I n . A . D . Mial l (ed) .

Canadian Soc . Petroleum Geo log i s t s Mem. v . 5,

p . 597-604.

M i a l l , A.D., 1985 - A r c h i t e c t u r a l - element a n a l y s i s • A new

methods of f a c i e s a n a l y s i s a p p l i e d t o f l u v i a l

d e p o s i t s . E a r t h . S c i . Rev. V, 2 2 , p . 261-308 .

Moss, A . J . , 1962 - The p h y s i c a l n a t u r e of common sandy and

pebbly d e p o s i t s . P a r t I Am. J o u r , S c i . , V. 260,

p . 337-373.

Moss, A , j . , 1963 - The p h y s i c a l n a t u r e of common sandy and

pebbly d e p o s i t s . Paurt I I , Am. j o u r . S c i , , V. 261,

p . 297-343.

i inyli , 1.2. '"' Kuiiti^. 1971 - ^f>n:=, and qlant r i pp le s in the

Ganga, Yamuna and Son Rivers, Uttar Pradesh, India,

Sedimentary Geol. V, 12, p . 53-66.

Sorby, K.C., 1859 - On the s t ruc tu res produced by the currents

present during the deposition of s t r a t i f i e d rocks .

Geologist, V. 2, p . 137-147.

Tewari, R.C., 1989 - Heavy Minerals from Late paleozoic Gondwana

sand stones of Giridih and adjoining basins, Bi'nar

with special reference t o shape ana lys i s of Zircons.

Bul le t in of Indian Geologists Associat ion, V. 1,

p . 19-26.

Todd, D.K., 1980 - Ground water Hydrology second Edition, Jhan.

Wiley and Sons, p . 5 35.

Visher , G.S., 1967a - Grain s ize d i s t r i bu t ions and deposi t ionai

process; P re -p r in t VII In te rna t iona l sedimentologic

Congress, Reading and Erinburg, England, p . 4 .

v i she r , G.S., 1967b - The r e l a t i o n of grain s ize t o sedimentary

processes (Abst) : Am, ASSO. Petrolleum Bul l , V, 51,

p . 489.

Visher, G.S., 1969 - Grain s ize d i s t r ibu t ions and deposi t ionai

p rocesses . Jour . Sed. Petrology, V. 39, p . 1077-1106

ino

W H 0, 1984 - Guidelines for Drinking water Ouallty, WHO,

ueneva.

William, G., I960 - Intrastratial flow and convolute folding

Geol. Mag, 208-214.